Sedimentology of a transgressive mixed‐energy (wave/tide‐dominated) estuary, Upper Devonian Geirud Formation (Alborz Basin, northern Iran)

Differentiate allogenic and autogenic controls on the formation of parasequences and depositional sequences of a tide‐ and wave‐dominated carbonate platform (Lower Cretaceous, Kopet‐Dagh Basin, Iran)

“…The bioclastic facies of the FD present a diverse fossil assemblage (brachiopods, bivalves, echinoderms, elongated orbitolines, and serpulids; and secondarily bryozoans, ostracods, and gastropods), which is indicative of open‐marine conditions. High diversity and abundance of the skeletal remains points to high benthic carbonate productivity with favourable water circulation, nutrient supply, light, and oxygenation in the middle ramp of the carbonate platform, between the FWWB and the storm‐weather wave base (Bachmann & Hirsch, 2006; Bover‐Arnal et al, 2009; Sharafi et al, 2016, 2021; Tucker & Wright, 1991; Wilmsen, Fürsich, et al, 2010; Wilmsen, Niebuhr, et al, 2010; Wilmsen, Niebuhr, & Hiss, 2005). The suitable conditions of the sedimentary environment led to the colonization of the substrate by trace makers, particularly endostratal deposit‐feeding and dwelling–feeding burrows Planolites , Scolicia , and Thalassinoides (Fürsich, Uchman, Alberti, & Pandey, 2018; Rodríguez‐Tovar et al, 2019; Rodríguez‐Tovar, Pérez‐Valera, & Pérez‐López, 2007).…”

“…Van Wagoner et al (1990) defined a parasequence as a conformable sedimentary package (several metres thick) of genetically related layers that is bounded by marine flooding surfaces and their correlative surfaces. Recognition of depositional sequences and parasequences, together with sea‐level interpretations of the Tirgan successions, was based on the sequential stratigraphic framework and corresponding terminology, in the way of Van Wagoner et al (1990), Vail, Audemard, Bowman, Eisner, and Pérez‐Cruz (1991), Catuneanu et al (2009, 2011), and Catuneanu (2019), further developed in related research (e.g., Bayet‐Goll et al, 2018; Bosence et al, 2009; Folkestad & Satur, 2008; Sharafi et al, 2016, 2019; Wilmsen, Fürsich, & Majidifard, 2013; Zecchin, 2007). In this sense, transgressive system tract (TST) sediments are normally characterized by a deepening‐ (and sometimes thinning‐) upward trend of a sedimentary package´s depositional sequence.…”

“…The effect of local and internal factors (e.g., tide‐dominated, wave‐dominated, or fluvial‐dominated sedimentary processes, oxygen level, water circulation, nutrient supply, local change in sedimentation rate) and local shifts in carbonate productivity can result in lateral changes of facies, the formation of internal erosional surfaces, change in the stacking pattern of the sedimentary packages, and the formation of the parasequences marked by minor flooding surfaces (e.g., Angulo & Buatois, 2012; Baniak, Gingras, Burns, & Pemberton, 2014; Bayet‐Goll et al, 2018; Belkhedim et al, 2019; Catuneanu, 2019; Plink‐Björklund, 2019). Large‐scale changes in facies belts, carbonate productivity zone, depositional environments, and even depositional systems—with the subsequent formation of the system tracts and medium–large‐scale cycles—are mainly controlled by allogenic factors, including tectonic regime (passive vs. active), eustatic, and climate changes (e.g., Belkhedim et al, 2019; Catuneanu, 2019; Sharafi et al, 2019; Sharafi, Longhitano, Mahboubi, Moussavi‐Harami, & Mosaddegh, 2016; Sharafi, Mahboubi, Moussavi‐Harami, Ashuri, & Rahimi, 2013; Sharafi, Mosaddegh, Bayet‐Goll, & Ahmadi, 2020). Such information is useful for the geological reconstruction of the sedimentary basins, in this case, the Kopet‐Dagh Basin, located in the northern margin of the Neo‐Tethys Ocean after its formation in the Middle Triassic period.…”

Dynamics and stratigraphy of a tidal sand ridge in the Bristol Channel (Nash Sands banner bank) from repeated high‐resolution multibeam echo‐sounder surveys

“…The processes operating during the lifetimes of tidal ridges and bars and their ultimate fates have been addressed through a combination of active monitoring (for example, time‐lapse bathymetric data, as here), sampling and geophysical surveys (Berné et al ., 1994, 1998; Fenies & Taslet, 1998; Reynaud et al ., 1999; Trentesaux et al ., 1999; Vecchi et al ., 2013; Franzetti et al ., 2015; Lockhart et al ., 2018), hydrodynamic modelling (De Vriend, 1990; Hulscher et al ., 1993; van Veelen et al ., 2018), and analyses of ancient examples preserved in cored subsurface sections (Folkestad and Satur, 2008; Schwarz et al ., 2011; Messina et al ., 2014; Wei et al ., 2018; Chiarella et al ., 2020) and in the rock record (Tillman & Martinsen, 1984; Gaynor & Swift, 1988; Mellere & Steel, 1995; Martinsen et al ., 1999; Yoshida, 2000; Plink‐Björklund & Steel, 2006; Plink‐Björklund, 2008; Steel et al ., 2008, 2012; Pontén & Plink‐Björklund, 2009; Hampson, 2010; Michaud, 2011; Martinius, 2012; Olariu et al ., 2012b; Scasso et al ., 2012; Chen et al ., 2014; López et al ., 2016; Michaud & Dalrymple, 2016; Sharafi et al ., 2016; Leszczyński & Nemec, 2020; Longhitano et al ., 2021). The latter potentially provide the finest spatial information but, before assessing it, confidence needs to be established that tidal ridges or bars have been correctly identified.…”

“…In the rock record, tidal ridge or bar deposits can be difficult to identify, although a number have been proposed (Tillman & Martinsen, 1984; Gaynor & Swift, 1988; Mellere & Steel, 1995; Martinsen et al ., 1999; Yoshida, 2000; Plink‐Björklund & Steel, 2006; Plink‐Björklund, 2008; Steel et al ., 2008, 2012; Pontén & Plink‐Björklund, 2009; Hampson, 2010; Michaud, 2011; Martinius, 2012; Olariu et al ., 2012b; Scasso et al ., 2012; Chen et al ., 2014; López et al ., 2016; Michaud & Dalrymple, 2016; Sharafi et al ., 2016; Longhitano et al ., 2021). In particular, there has been some debate concerning how tidal ridges can be discriminated from other tidally‐influenced deposits.…”