Discriminating ecological and evolutionary controls during the Ediacaran–Cambrian transition: Trace fossils from the Soltanieh Formation of northern Iran

Shahkarami, Setareh; Mángano, M. Gabriela; Buatois, Luís A.

doi:10.1016/j.palaeo.2017.03.012

Cited by 32 publications

(26 citation statements)

References 68 publications

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“…Eight facies have been recognized in Soltanieh Formation, which are grouped into siliciclastic-dominated and carbonatedominated facies associations (Shahkarami et al, 2017). The siliciclastic-dominated Facies Association comprises Facies Facies 1 consists of coarsening-upward cycles of interbedded greenish-gray silty shale and erosionally based, very fine-to medium-grained sandstone and sandy dolomite.…”

Section: Sedimentary Facies and Depositional Environmentmentioning

confidence: 99%

Ichnostratigraphy of the Ediacaran-Cambrian boundary: new insights on lower Cambrian biozonations from the Soltanieh Formation of northern Iran

2017

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Abstract.-Strata in the Central Alborz Mountains, northern Iran, are interpreted to show continuous sedimentation from Ediacaran through Cambrian times. The Soltanieh Formation consists of five members: Lower Dolomite, Lower Shale, Middle Dolomite, Upper Shale and Upper Dolomite members. The clastic units (Lower and Upper Shale members) represent sedimentation in distal marine settings, ranging from the shelf to offshore, and contain abundant trace fossils of biostratigraphic utility. Four ichnozones have been recognized. Ichnozone 1, containing Helminthoidichnites tenuis, Helminthopsis tenuis, and Cochlichnus anguineus, is early Fortunian based on small shelly fossils, and is interpreted as a distal expression of the Treptichnus pedum zone. Ichnozone 2, comprising the first occurrence of T. pedum, is middle Fortunian, and is best regarded as the upper half of the Treptichnus pedum Zone. Ichnozone 3 is late Fortunian-Cambrian Age 2, characterized by a sudden change in abundance and complexity of trace fossils. Main elements in this ichnozone include Cruziana problematica, Curvolithus isp., Phycodes isp., Treptichnus pedum, Treptichnus pollardi, and Treptichnus isp. Ichnozone 4 is of Cambrian Age 2-Age 3 and marked by the first appearances of Psammichnites gigas, Rusophycus avalonensis, and Didymaulichnus miettensis. Integration of trace fossils with small shelly fossils suggests that the Ediacaran-Cambrian boundary should be placed at the base of the Soltanieh Formation or within the Lower Dolomite Member. The delayed appearance of T. pedum and the low ichnodiversity in the Lower Shale and lower interval of the Upper Shale reflect limited colonization of settings below storm wave base during the early Fortunian.

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Section: Sedimentary Facies and Depositional Environmentmentioning

confidence: 99%

Ichnostratigraphy of the Ediacaran-Cambrian boundary: new insights on lower Cambrian biozonations from the Soltanieh Formation of northern Iran

2017

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“…Its stratigraphical range is lower Cambrian to Palaeogene (Osgood, 1970;Chlupáč, 1997;Jensen & Grant, 1998;Miller, 2001;Shahkarami et al, 2017). Recently, Belaústegui & Muñiz (2016) Material: Several specimens, preserved as horizontal broom-like or flabellate bundles (convex hyporelief) found on sandstone slabs at the Rakowice Małe Quarry.…”

Section: Fig 7gmentioning

confidence: 99%

Coniacian sandstones from the North Sudetic Synclinorium revisited: palaeoenvironmental and palaeogeographical reconstructions based on trace fossil analysis and associated body fossils

Chrząstek

Wypych

2018

Geologos

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The Coniacian quartz sandstones (Żerkowice Member, Rakowice Wielkie Formation) that crop out at quarries near Czaple-Nowa Wieś Grodziska (North Sudetic Synclinorium) contain a low-diversity assemblage of trace fossils:Gyrochorteisp.,Ophiomorpha nodosaLundgren, 1891,Ophiomorphaisp.,Phycodescf.curvipalmatum(Pollard, 1981), ?Phycodesisp.,Planolitescf.beverleyensis(Billings, 1862),Thalassinoides paradoxicusWoodward, 1830 and ?Thalassinoidesisp. Moreover, interesting compound burrow systems, here referred to asThalassinoides-Phycodescf.palmatusand ?Thalassinoides-Phycodes, were recognised at the Czaple Quarry. Additionally, ?Gyrochorteisp.,Phycodescf.flabellum(Miller and Dyer, 1878) and ?Treptichnusisp. were encountered at correlative levels in the Rakowice Małe Quarry. Some of these ichnotaxa have not been recorded previously from Coniacian sandstones of the Żerkowice Member. Additionally, in slabs of these sandstones, the gastropodNerinea bicinctaBronn, 1836 and the bivalveLima haidingeriZittel, 1866 were found. These interesting finds, in particular the gastropods, were already noted from the study area in the first half of the twentieth century by Scupin (1912–1913). Ethologically, the trace fossil assemblage is represented by domichnia or domichnia/fodinichnia (Ophiomorpha,Thalassinoides), fodinichnia (Phycodes) and pascichnia (Gyrochorte,Planolites). The compound burrow systems (Thalassinoides-Phycodes) are interpreted as dwelling/feeding structures. The possible tracemakers are crustaceans (Ophiomorpha,Thalassinoides) or worm-like animals (annelids and other) (Planolites, ?Phycodes,Gyrochorteand ?Treptichnus). The assemblage of trace fossils is characteristic of theSkolithosichnofacies andCruzianaichnofacies, typical of shallow-marine settings. Ichnological studies, as well as the presence of accompanying fossils (bivalves, gastropods), confirm the palaeoenvironmental reconstruction of the Żerkowice Member sandstones by Leszczyński (2010). That author interpreted the Coniacian sandstones as bar and storm deposits laid down in a shallow epicontinental sea (mainly the foreshore-upper shoreface; up to the middle shoreface) under normal oxygenation and salinity, in soft substrate, above fair-weather wave base. The deposition of the Żerkowice Member sandstones is linked to a regression that started after uplift of the southeastern part of the North Sudetic Synclinorium.

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“…Interestingly, the available studies integrating ichnological and sedimentological information within a sequence-stratigraphic framework suggest a more nuanced scenario, where trace-fossil distribution reveals a complex interplay of evolutionary and environmental controls (e.g. Shahkarami, Mángano & Buatois, 2017).…”

Section: A Critical Assessment Of the Utility Of Treptichnus Pedum Asmentioning

confidence: 99%

“…The common absence of T. pedum in settings below storm wave base may reflect the seaward boundary of its habitat or a preservational bias resulting from the lack of lithological heterogeneities (Shahkarami, Mángano & Buatois, 2017). The latter is supported by the presence of T. pedum in thin siltstone layers intercalated in a shale succession formed right below storm wave base in the Soltanieh Formation of Iran (Shahkarami, Mángano & Buatois, 2017).…”

Section: A Critical Assessment Of the Utility Of Treptichnus Pedum Asmentioning

confidence: 99%

Treptichnus pedumand the Ediacaran–Cambrian boundary: significance and caveats

Buatois

2017

Geol. Mag.

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The Ediacaran–Cambrian (E-C) boundary is based on the first appearance of the ichnofossilTreptichnus pedum. Investing an ichnotaxon with such biostratigraphic pre-eminence has been the focus of criticism. Points of contention have revolved around four main issues: (1) ichnotaxonomy, (2) behavioural significance, (3) facies controls and (4) stratigraphic occurrence. First, confusion results from the fact thatTreptichnus pedumwas originally referred to asPhycodes pedumand, more recently, some authors have placed it inTrichophycusorManykodes. However, the overall geometry of these burrows indicates they belong inTreptichnus.Second, regardless of its precise mode of feeding, the behaviour involved is iconic of the Cambrian explosion. Third, objections are based on the idea that trace fossils show a closer link to facies than body fossils. Notably, in contrast to common assumptions,T. pedumis not only present in the low-energy offshore of wave-dominated marine settings, but it occurs at considerably shallower water in intertidal and shallow-subtidal zones of tide-dominated systems, as well as in mouth bars of deltaic systems and lower shoreface to offshore transition zones of wave-dominated marine settings. Its broad environmental tolerance supports evolutionary innovations rather than facies controls as the main mechanism underlying the observed vertical pattern of distribution ofT. pedumin most E-C successions comprising shallow-marine deposits. Fourth, although treptichnids have been documented below the E-C boundary,T. pedumis not known from Ediacaran rocks. The delayed appearance ofT. pedumin E-C successions should be analysed on a case-by-case basis.

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Discriminating ecological and evolutionary controls during the Ediacaran–Cambrian transition: Trace fossils from the Soltanieh Formation of northern Iran

Cited by 32 publications

References 68 publications

Ichnostratigraphy of the Ediacaran-Cambrian boundary: new insights on lower Cambrian biozonations from the Soltanieh Formation of northern Iran

Ichnostratigraphy of the Ediacaran-Cambrian boundary: new insights on lower Cambrian biozonations from the Soltanieh Formation of northern Iran

Coniacian sandstones from the North Sudetic Synclinorium revisited: palaeoenvironmental and palaeogeographical reconstructions based on trace fossil analysis and associated body fossils

Treptichnus pedumand the Ediacaran–Cambrian boundary: significance and caveats

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