Silurian sea-level fluctuations

Ross, Charles A.; Ross, June R. P.

doi:10.1130/0-8137-2306-x.187

Cited by 37 publications

(64 citation statements)

References 14 publications

(18 reference statements)

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“…This study replicates the approach applied to North American datasets by Johnson (1987) and 360 first attempted on a global scale by McKerrow (1979), prior to the influential studies of value, those of Ross and Ross (1996), , Artyushkov and Chekhovich 398 (2001) and Haq and Schutter (2008) being notable exceptions. This use of varied criteria 399 emphasises the need, when seeking to identify correlatable events, to focus on abrupt changes 400 and gross trends rather than to compare precise profiles.…”

mentioning

confidence: 63%

“…The 439 suspicion also emerges (see below) that some of the most commonly used curves are over-440 reliant on the data from a single region (e.g. Ross and Ross, 1996) and/or are a conflation of 441 higher and lower order base level events, but are fully representative of neither.…”

mentioning

confidence: 99%

“…Ross and Ross (1996;also Page et al, 2007) restrict 463 it to the convolutus Biozone. Others, by recognising its peak in the mid Aeronian leptotheca 464 Biozone (e.g.…”

mentioning

confidence: 99%

“…Ross and Ross, 1996;Page et al, 447 2007) or close to the revolutus-triangulatus biozonal boundary (e.g. Johnson, 1996Johnson, , 2010.…”

mentioning

confidence: 99%

“…Ross and Ross, 1996), imply a wider significance for the basal 456 sedgwickii Biozone flooding surface (9). The late sedgwickii-halli biozonal interval is widely 457 recognised as a period of falling sea levels, shown by Johnson (1996), Ross and Ross (1996) 458 and Page et al (2007) to have reached its acme close to the base of the guerichi Biozone (F).…”

mentioning

confidence: 99%

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Gauging the impact of glacioeustasy on a mid-latitude early Silurian basin margin, mid Wales, UK

Davies

Waters

Molyneux

et al. 2016

Earth-Science Reviews

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mentioning

confidence: 63%

mentioning

confidence: 99%

“…Ross and Ross (1996;also Page et al, 2007) restrict 463 it to the convolutus Biozone. Others, by recognising its peak in the mid Aeronian leptotheca 464 Biozone (e.g.…”

mentioning

confidence: 99%

“…Ross and Ross, 1996;Page et al, 447 2007) or close to the revolutus-triangulatus biozonal boundary (e.g. Johnson, 1996Johnson, , 2010.…”

mentioning

confidence: 99%

mentioning

confidence: 99%

See 3 more Smart Citations

Gauging the impact of glacioeustasy on a mid-latitude early Silurian basin margin, mid Wales, UK

Davies

Waters

Molyneux

et al. 2016

Earth-Science Reviews

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Structural, Reverse‐Basin and Forward Stratigraphic Modelling of the Southern Cantabrian Basin, Northwest Spain

Veselovský¹,

Bechstädt

Zühlke

2008

Analogue and Numerical Modelling of Sedimentary Systems: From Understanding to Prediction

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The evolution of the Palaeozoic Southern Cantabrian Basin is quantified by a multidisciplinary approach of structural balancing, reverse-basin and forward stratigraphic modelling. These methods were applied to the N-S trending, 54 km long Bernesga Transect in the Cantabrian Mountains. Total tectonic shortening of the Southern Cantabrian Basin amounted to a minimum of 54%. These data were derived from two-dimensional structural balancing of the deformed basin infill. Two-dimensional reverse-basin modelling was used for analysing the evolution of the basin architecture, considering lithofacies, incremental compaction, eustatic sea-level changes and flexural loading of the crust. The model comprises the entire basin infill between the top of the Neoproterozoic basement and the time of maximal burial (Cenozoic). Six major subsidence trends, with time spans between 9 and 65 Myr, subdivide the long-term evolution of accommodation space in time. These trends reflect different lithospheric configurations prior to, during and after the Variscan Orogeny, having been primarily triggered by major changes in thermo-tectonic and flexure-induced subsidence, as well as by regional and extraregional tectonics. Basin modelling permits the identification of two encroachment subcycles during the Silurian and Devonian, as well as the approach of the Variscan orogenic front in the Early Carboniferous. The latter is reflected by migrating, strongly subsiding depocentres (orogenic foredeep), controlled by increased flexural-induced and thermo-tectonic subsidence. Two-dimensional stratigraphic forward modelling was used to simulate the evolution of the Southern Cantabrian Basin, and to quantify internal and external parameters governing deposition (e.g. sediment transport, sedimentation rates, in-situ carbonate production, erosion and compaction). The model includes data from the Neoproterozoic to the Lower Carboniferous with a focus on the Devonian. Carbonate factories in the Devonian were controlled by fluctuating siliciclastic input and differential thermo-tectonic subsidence, and subordinately influenced by eustatic sea-level changes. Decompacted carbonate production rates reach up to 780 m Myr −1 . The changes in carbonate production rates mirror the drift of Iberia from cooler to subtropical/tropical conditions during Devonian times.

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Upper Ordovician-Lower Silurian transgressive-regressive cycles of the Central Iberian Zone (NE Jaén, Spain)

2005

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A thick Upper Ordovician shelf sequence was developed in the northern Gondwana margin (southernmost exposures of the Central Iberian Zone). Integrated sedimentologic and stratigraphic studies allow distinction between pedogenetic processes (Facies association C), shoreline deposits (Facies association S), proximal to distal shelf (Facies association L, H 1 , H 2 , H 3 ) and outer shelf zone or open marine environments (Facies association M, Mo). The vertical distribution of facies is characterized by the presence of regressive high frequency sequences (partial shelf progradational sequences), affected by the presence of catastrophic phenomena (storms). These sequences, in turn, can be classified into higher-order transgressive (T)-regressive (R) cycles.Two second-order T-R megacycles (MC. Ord-2 and MC. Sil-1) limited by a major sequence boundary are identified. Traces of emersion (palaeokarsts and palaeosols) are detected along the sequence boundary, and these are related to the eustatic sealevel fall that occurred during the Ashgillian.The MC. Ord-2 and MC. Sil-1 megacycles extend respectively from the Middle Arenig to the Ashgillian and from Late Ashgillian to the Late Llandovery. Major transgressive peaks occurred at the Llanvirn and at the Middle Llandovery (Aeronian). The vertical distribution of the facies delineates successive genetically related units in relation to relative sea-level changes. Within the upper part of the first megacycle (MC. Ord-2) six third-order cycles are proposed (Lla-1, Car-1, Car-2, Car-3, Car-4, Ash-1), in which a transgressive and a regressive interval can be distinguished. Within the lower part of the second megacycle (MC. Sil-1) two transgressive-regressive third-order cycles are proposed (Lly-1, Lly-2).

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Silurian sea-level fluctuations

Cited by 37 publications

References 14 publications

Gauging the impact of glacioeustasy on a mid-latitude early Silurian basin margin, mid Wales, UK

Gauging the impact of glacioeustasy on a mid-latitude early Silurian basin margin, mid Wales, UK

Structural, Reverse‐Basin and Forward Stratigraphic Modelling of the Southern Cantabrian Basin, Northwest Spain

Upper Ordovician-Lower Silurian transgressive-regressive cycles of the Central Iberian Zone (NE Jaén, Spain)

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