Storm effects on siliciclastic and carbonate shelf sediments in the medial Silurian succession of Pennsylvania

Cotter, Edward

doi:10.1016/0037-0738(90)90052-u

Cited by 15 publications

(17 citation statements)

References 27 publications

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“…Earth Sci. Downloaded from www.nrcresearchpress.com by UNIV CHICAGO on 11/19/14 storm wave base (see Kreisa 1981;Aigner 1985;Cotter 1990) ( Table 2). Similar low-angle lamination is common in the lower shoreface but is commonly reworked by fair-weather processes (Howard and Reineck 1972).…”

Section: Parallel-laminated Dolostonementioning

confidence: 98%

“…The widespread lateral distribution of this graded, erosively based bed suggests a storm origin. The rare large ripples at the top of the bed are interpreted as storm-generated coarse-grained wave ripples (Leckie 1988) or "pararipples" (Brookfield and Brett 1988;Cotter 1990). The coarse-grained ripples in this facies commonly only modify the tops of the beds, leaving earlier-formed internal sedimentary structures …”

Section: Fig 8 Trough-cross-bedded Dolostone Facies (A) Arrows Bramentioning

confidence: 99%

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Sedimentology of an Early Silurian carbonate ramp: the Manitoulin Formation, southern Ontario

Anastas¹,

Coniglio²

1993

Can. J. Earth Sci.

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The Manitoulin Formation is a pervasively dolomitized Lower Silurian carbonate unit that was deposited in the Michigan Basin and locally in the Appalachian Basin. The formation reaches a maximum thickness of 11.1 m in southern Ontario and can be subdivided into eight facies and four regionally correlatable facies assemblages. Owing to the relatively continuous transition of shallow to deeper water facies from the northern to southern portions of the study area, the Manitoulin Formation is interpreted as having formed on a carbonate ramp with a southerly component of dip. Our study suggests that the Algonquin Arch, which is transected by the outcrop belt, did not significantly influence deposition or separate the Michigan and Appalachian basins.Depending on its location on the ramp, the Manitoulin Formation shows evidence of varying degrees of episodic storm events alternating with fair-weather processes such as wave shoaling, sediment reworking, and bioturbation. Apart from bioturbation, these fair-weather processes became less prevalent to the south. The gently dipping antecedent topography, the temporary lack of frame-builders, and a shallow basin setting led to the creation of a carbonate ramp rather than a rimmed shelf.La Formation de Manitoulin est une unite de carbonates profondement dolomitisbe, appartenant Silurien infbrieur, qui fut dCposbe dans le bassin de Michigan et localement dans le bassin des Appalaches. L'Cpaisseur maximale de la formation de 11,l m fut atteinte dans le sud de l'ontario, oG la formation est subdiviske en huit faciks dont quatre assemblages faciologiques, peuvent &tre regionalement mis en correlation. Vu la transition relativement continue, du nord vers le sud, des facibs de faible tranche d'eau i eau profonde dans la rCgion etudiCe, la Formation de Manitoulin est interprCt6e comme Ctant form6 sur une rampe de carbonates avec pendage vers le sud. Notre ktude suggbre que l'arc Algonquin, lequel est coup6 transversalement par la zone d'affleurements, n'a pas influencC significativement la ~Cdimentation ou sCparC le bassin de Michigan du bassin des Appalches.Selon l'endroit sur la rampe, la Formation de Manitoulin exhibe, B divers degrb, des indices d'kvknements de tem$tes Cpisodiques alternant avec des processus de temps calme tels les effets des vagues sur haut-fond, le remaniement des sediments et la bioturbation. Hormis la bioturbation, ces processus de temps calme etaient devenus moins actifs au sud. La topographie antecuente de faible pendage, l'absence temporaire d'organismes constructeurs, et le contexte d'un bassin peu profond ont favoris6 le dCveloppement d'une rampe de carbonates plut6t qu'une plate-forme frangee.[Traduit par la rkdaction]Can.

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Section: Parallel-laminated Dolostonementioning

confidence: 98%

Section: Fig 8 Trough-cross-bedded Dolostone Facies (A) Arrows Bramentioning

confidence: 99%

Sedimentology of an Early Silurian carbonate ramp: the Manitoulin Formation, southern Ontario

Anastas¹,

Coniglio²

1993

Can. J. Earth Sci.

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“…Above storm wave base, very fine-grained sand introduced by storms was reworked into varieties of wave-generated ripple forms by late-stage oscillation related to the same storms (De Raaf et at., 1977;Pedersen, 1985;Driese et al, 1991;Davis and Byers, 1993;Brenchley et at., 1993;Krassay, 1994;Colquhoun, 1995). Thin and medium interbeds of flat-laminated and/or hummocky cross-stratified sandstone are storm beds ('tempestites') deposited above storm wave base (Aigner, 1985;Brenchley, 1985;Cotter, 1990;Brenchley et at., 1993;Myrow and Southard, 1991;. In the anoxic conditions characteristic of shallowmarine shelves in the Late Devonian (see above), bioturbators were largely absent, thereby enabling preservation of many fine, process-indicating details.…”

Section: Facies Of the Lower Witteberg Group Facies 1 -Mudrock And Wamentioning

confidence: 99%

Depositional setting and cyclic development of the lower part of the Witteberg Group (Mid- to Upper Devonian), Cape Supergroup, Western Cape, South Africa

Cotter

2000

South African Journal of Geology

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Mid-to Upper Devonian strata of the lower Witteberg Group in the Cape Fold Belt of South Africa comprise three principal facies deposited in the shoreface and contiguous inner shelfalong a storm-dominated coastal zone. Weakly burrowed mudrock with variable minor proportions of wave-rippled sandstone (linsen, flasers, hummocky cross stratification [HCSJ) (facies 1) accumulated in the inner shelf below, near, and just above storm wave base. Very fine-and finegrained sandstone that displays flat and wavy lamination and HCS, as well as compound wave-ripple lamination (facies 2), was deposited in the lower shoreface above fair-weather wave base. Fine-to coarse-grained sandstone containing crosslamination, anisotropic HCS, and compound wave-ripple lamination (facies 3) formed in the mid to upper shoreface. Regionally, lower Witteberg strata change from proportionally more facies 2 and 3 at proximal (northern) sites to mostly facies 1 at distal (southern) sites. The lower Witteberg Group consists of approximately 40 shallowing-upward facies sequences (parasequences) whose average thickness is approximately 12 m. These are grouped into progradational parasequence sets of up to 10 parasequences each for a total of approximately 3.5 parasequence sets in the lower Witteberg. The lowest parasequence set extends from the base of the Karoopoort Formation (top of underlying Bokkeveld Group) and culminates at the top of the Blinkberg Formation in the Witteberg Group, and approximately 2.5 parasequence sets make up the overlying Swartruggens Formation. The characteristics and stratigraphic architecture of the lower Witteberg Group are consequences of the interaction oftwo different orders of global sea-level fluctuation. The lower Witteberg parasequences had a periodicity between 250 and 300 ka, within the Milankovitch range, and their character and mean thickness are very similar to cyclic patterns recorded in contemporaneous Givetian-Frasnian siliciclastic and carbonate strata on four other continents. The progradational parasequence sets had a mean recurrence interval in the order of 3.0 Ma and can be correlated with specific third-order fluctuations of global sea-level proposed for contemporaneous Upper Devonian strata in Euramerica. This reinforces assignment of the age of the lower Witteberg as extending from the mid-Givetian Stage to the end of the Frasnian Stage.

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“…2). In North America, research by Smith (1970) and Cotter (1983Cotter ( , 1990) details the changing position of Taconia's early Silurian shoreline to the present south in New York State and Pennsylvania (Fig. 1).…”

Section: Comparison Of Onshore-offshore Profiles and Paleogeographymentioning

confidence: 99%

“…Storm cycles, indicated by amalgamated sandstones with traces of swaley cross-stratification, form part of the Gadsden sequence in Alabama. Storm activity also is registered by the nearshore Silurian sands and carbonates of central Pennsylvania (Cotter, 1990). Elsewhere on the Laurentian platform, carbonates with common preservation of pentamerid brachiopods in crowded growth position are not as suggestive of persistent storm activity, except for the fact that large populations of articulated shells are usually truncated by scour surfaces.…”

Section: Comparison Of Lower Silurian Shores and Shelves North Amerimentioning

confidence: 99%

Comparison of Lower Silurian shores and shelves in North America and Siberia

Johnson¹,

Tesakov²,

Predtetchensky³

et al. 1997

Paleozoic Sequence Stratigraphy, Biostratigraphy, and Biogeography: Studies in Honor of J. Granville ("Jess") Johnson

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Storm effects on siliciclastic and carbonate shelf sediments in the medial Silurian succession of Pennsylvania

Cited by 15 publications

References 27 publications

Sedimentology of an Early Silurian carbonate ramp: the Manitoulin Formation, southern Ontario

Sedimentology of an Early Silurian carbonate ramp: the Manitoulin Formation, southern Ontario

Depositional setting and cyclic development of the lower part of the Witteberg Group (Mid- to Upper Devonian), Cape Supergroup, Western Cape, South Africa

Comparison of Lower Silurian shores and shelves in North America and Siberia

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