Tidal/littoral offshore shelf deposits—Lower Cambrian Gog Group, southern Rocky Mountains, Canada

Hein, Frances J.

doi:10.1016/0037-0738(87)90060-1

Cited by 16 publications

(13 citation statements)

References 18 publications

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“…Also, Cambrian continental shelves were wide shallow platforms which would have amplified semi‐diurnal tides (Clarke & Battisti, 1980), as well as having a high potential for tidal resonance (Willis, 2005). Whilst no numerical model was attempted in the present study to estimate a precise tidal range, the Gog Group is interpreted to have been deposited on a tide‐dominated shelf (Hein, 1987; Desjardins et al. , 2010a).…”

Section: Geological Settingmentioning

confidence: 93%

“…Most of these transgressive Cambrian sandstone units are considered to have been deposited under the influence of strong tidal currents, because coastal facies locally contain diagnostic features such as herringbone cross‐stratification, lenticular/wavy/flaser bedding, double mud drapes and tidal bundles. It has been argued that the effects of tides were much greater on Cambrian continental shelf areas, because the presumed closer position of the Moon to the Earth increased tidal forces (Hein, 1987). Also, Cambrian continental shelves were wide shallow platforms which would have amplified semi‐diurnal tides (Clarke & Battisti, 1980), as well as having a high potential for tidal resonance (Willis, 2005).…”

Section: Geological Settingmentioning

confidence: 99%

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Sedimentological–ichnological model for tide‐dominated shelf sandbodies: Lower Cambrian Gog Group of western Canada

Desjardins

Buatois²,

Pratt³

et al. 2012

Sedimentology

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Dunes and bars are common elements in tide‐dominated shelf settings. However, there is no consensus on a unifying terminology or a systematic classification for thick sets of cross‐stratified sandstones. In addition, their ichnological attributes have hardly been explored. To address these issues, the properties, architecture and ichnology of compound cross‐stratified sandstone bodies contained in the Lower Cambrian Gog Group of the southern Canadian Rocky Mountains are described here. In these transgressive sandstones, five types of compound cross‐stratified sandstone are distinguished based on foreset geometry, sedimentary structures and internal heterogeneity. These represent four broad categories of subtidal sandbodies: (i) compound‐dune fields; (ii) sand sheets; (iii) sand ridges; and (iv) isolated dune patches; tidal bars comprise a fifth category but are not present in the Gog Group. Compound‐dune fields are characterized by sigmoidal and planar cross‐stratified sandstone in coarsening‐upward and thickening‐upward packages (Type 1); these are mostly unburrowed, or locally contain representatives of the Skolithos ichnofacies, but are intercalated with intensely bioturbated sandstone containing the archetypal Cruziana ichnofacies. Sand‐sheet complexes, also composed of compound dunes, cover more extensive subtidal areas, and comprise three adjacent subenvironments: core, front and margin. The core is characterized by thick‐bedded sets of cross‐stratified sandstone (Type 2). A decrease of bedform size at the front is recorded by wedges of thinner‐bedded, low‐angle and planar cross‐stratified sandstone (Type 3) exhibiting dense Skolithos pipe‐rock ichnofabric. The margin is characterized by interbedded sandstone and mudstone, and hummocky cross‐stratified sandstone. Sand‐sheet deposits exhibit clear trends in trace‐fossil distribution along the sediment transport path, from non‐bioturbated beds in the core to Skolithos ichnofacies at the front, and a depauperate Cruziana ichnofacies at the margin. Tidal sand ridges are large elongate sandbodies characterized by large sigmoid‐shaped reactivation surfaces (Type 4). Sand ridges display clear ichnological trends perpendicular to the axis of the ridge, with no bioturbation or a poorly developed Skolithos ichnofacies in the core, a depauperate Cruziana ichnofacies in lee‐side deposits, and Cruziana ichnofacies at the margin. While both tidal ridges and tidal bars migrate by means of lateral accretion, the latter occur in association with channels while the former do not. Because tidal bars tend to occur in brackish‐water marginal‐marine settings, their ichnofauna are typically of low diversity, representing a depauperate Cruziana ichnofacies. Isolated dune patches developed on sand‐starved areas of the shelf, and are represented by lenticular sandbodies with sigmoidal reactivation surfaces (Type 5); they typically lack trace fossils, but the interfingering muddy deposits are intensely bioturbated by a high‐diversity fauna recording the Cruziana ichnofacies....

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Section: Geological Settingmentioning

confidence: 93%

Section: Geological Settingmentioning

confidence: 99%

Sedimentological–ichnological model for tide‐dominated shelf sandbodies: Lower Cambrian Gog Group of western Canada

Desjardins

Buatois²,

Pratt³

et al. 2012

Sedimentology

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“…Hein, 1987) and show an upward increase in flow energy (dune and grain sizes) indicating an aggradational shallowing culminating in the reworking by sea waves (Figures 6 and 9) after reaching the fairweather wave base. Hein, 1987) and show an upward increase in flow energy (dune and grain sizes) indicating an aggradational shallowing culminating in the reworking by sea waves (Figures 6 and 9) after reaching the fairweather wave base.…”

Section: Basin-axis Tidal Barsmentioning

confidence: 99%

Sedimentation in a synclinal shallow‐marine embayment: Coniacian of the North Sudetic Synclinorium, SW Poland

Leszczyński

Nemec

2019

The Depositional Record

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This study is a reconstruction of the Coniacian palaeogeographic and palaeoenvironmental development in the North Sudetic Basin, a synclinal trough within the Late Cretaceous Central European seaway linking the Boreal and Tethyan marine provinces. The basin formed as an early side effect of the Alpine orogeny combined with the mid-Cretaceous eustasy, and crucial stages of its evolution occurred during the Coniacian. The basin in the early Coniacian was a long and narrow shallow-marine embayment with a hypothetical (non-preserved) bayhead strait funnelling tidal currents. Coalescing tidal sand ridges formed a littoral platform that prograded from the bayhead zone along the basin axis, impinged on laterally by the basin-margin shoreface and local river deltas. A mid-Coniacian forced marine regression and closure of the bayhead strait, attributed to the Alpine tectonism combined with eustasy, brought about a dramatic change in the basin, whereby the basin-wide littoral sand platform emerged and turned briefly into a denudated coastal plain. The late Coniacian eustatic marine transgression formed an in-place growing coastal sand barrier at the outer edge of the former littoral platform, sheltering a paralic limno-lagoonal plain with peat-forming mires. The coastal barrier was eventually drowned by the sea and maximum marine flooding occurred, followed by a normal regression recorded as a rapidly upwards-shallowing succession of offshore-transition to fluvio-deltaic deposits. This case study of the sedimentation pattern in an evolving, tectonically controlled marine embayment contributes to the existing facies models for estuarine embayments formed by a passive marine drowning of large fluvial or glacial valleys. K E Y W O R D SIchnofacies, lithofacies, North Sudetic Basin, paralic plain, shoal-water deltas, shoreface, tidal sand ridges

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“…Des séquences cycliques sont associées à l'influence des facteurs allocycliques sur la sédimentation (Edwards et al, 2005;Eriksson et al, 2001;Hall et al, 2005;Hein, 1987;Hunter and Clifton, 1982;Martins-Neto et al, 2001;Mishra et al, 2004;Mueller et al, 1994). Cependant, dans les deltas il est difficile de séparer le contrôle allocyclique du contrôle autocyclique sur la sédimentation selon Bhattacharya et Walker (1992).…”

Section: 22-changements Latéraux Et Verticaux De Facièsunclassified

“…Groupe de Timiskaming :-LB Formation de la Bruyère T Formation de Granada, C Groupe de Cadillac, P Groupe de Pontiac, B groupe de Blake River. Littérature importante (Bouma, 1962;Walker, 1978;Lowe, 1982;Walker, 1984;Lowe, 1997;Shanmugam, 1997) (Lowe, 1982 Lowe, 1988;Lowe, 1997;Shanmugam, 1997) ( Harms et al, 1975;Hamblin et Walker, 1979;Dott et Bourgeois, 1982;Dott et Bourgeois, 1983;Bose et Das, 1986;Hein, 1987;Monaco, 1992;Colquhoun, 1995;Makhlouf, 2002) (SepkoskiJr, 1982;Nemec et al, 1984; Plint étal, 1992;Eyles, 1994;Datta, 1998;Dattae*a/., 1999; Edwards étal, 2005;Mueller et Pickett, 2005) (Kano, 1991LajoieetStix, 1992; Bleeker et al, 1999;Mueller et al, 2000a) (Reineck et Singh, 1975) (Miall, 1978Miall, 1982;Miall, 1985;Reineck et Singh, 1986;Amireh et al, 1994Amireh et al, .2001 Chapitre 2. Analyse volcano-sédimentaire (Miall, 1978;Miall, 1982;Miall, 1985) (Heward, 1978Miall, 1978;Heward, 1982;Miall, 1982;…”

unclassified

Caractéristiques sédimentologiques, volcanologiques et structurales du bassin de Granada dans la ceinture de roches vertes de l'Abitibi (Québec) /

Diop¹

2011

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The Granada Basin, correspond to the stratigraphie unit known as the Granada Formation. This unit lies in the southernmost part of the Southern Volcanic Zone of the greenstone dominated Abitibi Subprovince in Quebec.Faciès analysis in the Granada Basin has identified clastic and volcaniclastic rocks deposited in an environment evolving from relatively deep marine to fluvial. The earliest sediments were mainly turbidites (faciès la and lb) deposited in extensional sub-basins. These sediments were overlain by a regressive sequence that evolved from shallow marine wave base dominated sediments (faciès 2a) to coastal deposits (faciès 2b). These deposits represent the transition between marine and continental depositional environments. The transition zone is marked by deposits of sandstoneargillites-stratified pebble conglomerate (faciès 2b) transported by waves and tides between the subtidal and intertidal zone. Faciès 3a and 3b of the felsic volcaniclastic lithofacies are interbedded with faciès la, lb and 2a.Deposits of the Granada Basin are transitional faciès separated by intra-basin unconformities, which are characteristic of sedimentary basins formed along fault margins. The volcano-sedimentary deposits of the Granada Basin have characteristics of sedimentation influenced by tectonisme such as: i) local and basinwide lateral and vertical faciès variations; ii) alternating fining and coarsening upwards sequences; iii) high rate of accumulation of sediments; iv) some conglomerate boulders are over 1 m in size and the thickness of conglomerate deposits; v) interdigitation of conglomerates and sandstones that denotes a progradation; vi) intra-basin unconformities; vii) the local source of conglomerates; and viii) associated alkaline magmatism. Tectonism would be ongoing throughout the development of the basin which would have induced several phases of source renewal areas for the sediments coupled with intra-basin unconformities. The earliest formed sedimentary deposits of the Granada Basin were affected by uplift and subsequently eroded and recycled into later basin fill along intra-basin unconformities. Gradually as the basin filled the sedimentary deposits became less and less shallower which is a characteristic of piggyback-type basins. The decrease in the depth is a consequence of an increase in topography due to repeated uplift along faults.Sedimentary rocks of the Granada Basin were intruded by alkalic mature volcanic arc-type sills, stocks and porphyritic dikes. These intrusive rocks are similar to Timiskaming-type porphyry intrusions and volcanic rocks found in the Kirkland Lake area of Ontario.The structural style of the Granada Basin, consisting of overturned southward verging tight to isoclinal folds, is characteristic of thrust basins. Two major east-west trending synclinal axial traces are distinguishable and their juxtaposition in a back to back relationship is compatible with there being an unconformity between them. This unconformity is further demonstrated by the presence of sandstone cla...

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Tidal/littoral offshore shelf deposits—Lower Cambrian Gog Group, southern Rocky Mountains, Canada

Cited by 16 publications

References 18 publications

Sedimentological–ichnological model for tide‐dominated shelf sandbodies: Lower Cambrian Gog Group of western Canada

Sedimentological–ichnological model for tide‐dominated shelf sandbodies: Lower Cambrian Gog Group of western Canada

Sedimentation in a synclinal shallow‐marine embayment: Coniacian of the North Sudetic Synclinorium, SW Poland

Caractéristiques sédimentologiques, volcanologiques et structurales du bassin de Granada dans la ceinture de roches vertes de l'Abitibi (Québec) /

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