“…Sedimentary environment: Archaeonassa, Lockeia, Skolithos and Protovirgularia are usually interpreted as characteristic of shallow environments, from nearshore to lower offshore (Uchman et al 2004a;Bradshaw 2010;Cabrera and Olivero 2011;Nagel et al 2013;Olivero and Cabrera 2013) but they also appear in deep-sea settings (Uchman 2004;Poursoltani et al 2007;Wetzel et al 2007;Zhang et al 2008;Nara and Ikari 2011;Uchman and Rattazzi 2011;Greene et al 2012). They are also known from marginal-marine and freshwater settings (McIlroy 2004b;Carmona et al 2009;Buatois and Mángano 2011;Gingras et al 2011;Melchor et al 2012b;Scott et al 2012).…”
The following trace fossils have been recognised in the Lower Muschelkalk of Raciborowice Gorne (North Sudetic Synclinorium, SW Poland): Archaeonassa fossulata, Balanoglossites triadicus, ?Gastrochaenolites isp., Lockeia isp., Palaeophycus tubularis, Palaeophycus isp., ?Planolites beverleyensis, P. montanus, Planolites isp., ?Protovirgularia isp., Rhizocorallium commune var. auriforme, R. commune var. irregulare, R. jenense, Skolithos linearis, Thalassinoides suevicus and Trypanites weisei. Coprolites and an unidentified trace fossil A are also described. The trace fossils allow the discrimination of five ichnoassociations in the Raciborowice Gorne section: (IA 1) Rhizocorallium- Pholeus, (IA 2) Rhizocorallium-Palaeophycus, (IA 3) Thalassinoides, (IA 4) Trypanites-Balanoglossites and (IA 5) Planolites-Palaeophycus. The Lower Muschelkalk succession was deposited on a shallow carbonate ramp affected by frequent storms. Deposition commenced with sedimentation in a restricted lagoon on the inner ramp with a short episode of sabkha formation. It continued on the middle and outer ramp and then on a skeletal shoal of the outer ramp and in an open basin. Ichnoassociation IA 5 is related to a maximum transgression that commenced with the deposition of the Spiriferina Bed and which probably marked the opening of the Silesian-Moravian Gate. The basin underwent two shallowing episodes, as evidenced by ichnoassociations IA 3-IA 4, resulting in the formation of hardgrounds. Bathymetric changes in the Raciborowice Gorne section correspond well with a general transgressive trend in the Germanic Basin.
“…Sedimentary environment: Archaeonassa, Lockeia, Skolithos and Protovirgularia are usually interpreted as characteristic of shallow environments, from nearshore to lower offshore (Uchman et al 2004a;Bradshaw 2010;Cabrera and Olivero 2011;Nagel et al 2013;Olivero and Cabrera 2013) but they also appear in deep-sea settings (Uchman 2004;Poursoltani et al 2007;Wetzel et al 2007;Zhang et al 2008;Nara and Ikari 2011;Uchman and Rattazzi 2011;Greene et al 2012). They are also known from marginal-marine and freshwater settings (McIlroy 2004b;Carmona et al 2009;Buatois and Mángano 2011;Gingras et al 2011;Melchor et al 2012b;Scott et al 2012).…”
The following trace fossils have been recognised in the Lower Muschelkalk of Raciborowice Gorne (North Sudetic Synclinorium, SW Poland): Archaeonassa fossulata, Balanoglossites triadicus, ?Gastrochaenolites isp., Lockeia isp., Palaeophycus tubularis, Palaeophycus isp., ?Planolites beverleyensis, P. montanus, Planolites isp., ?Protovirgularia isp., Rhizocorallium commune var. auriforme, R. commune var. irregulare, R. jenense, Skolithos linearis, Thalassinoides suevicus and Trypanites weisei. Coprolites and an unidentified trace fossil A are also described. The trace fossils allow the discrimination of five ichnoassociations in the Raciborowice Gorne section: (IA 1) Rhizocorallium- Pholeus, (IA 2) Rhizocorallium-Palaeophycus, (IA 3) Thalassinoides, (IA 4) Trypanites-Balanoglossites and (IA 5) Planolites-Palaeophycus. The Lower Muschelkalk succession was deposited on a shallow carbonate ramp affected by frequent storms. Deposition commenced with sedimentation in a restricted lagoon on the inner ramp with a short episode of sabkha formation. It continued on the middle and outer ramp and then on a skeletal shoal of the outer ramp and in an open basin. Ichnoassociation IA 5 is related to a maximum transgression that commenced with the deposition of the Spiriferina Bed and which probably marked the opening of the Silesian-Moravian Gate. The basin underwent two shallowing episodes, as evidenced by ichnoassociations IA 3-IA 4, resulting in the formation of hardgrounds. Bathymetric changes in the Raciborowice Gorne section correspond well with a general transgressive trend in the Germanic Basin.
“…Throughout the formation, abundant and diverse microfossils, invertebrates, vertebrates, and plants occur in a number of fossiliferous horizons (Feldmann & Woodburne 1988, Stilwell & Zinsmeister 1992, Gaździcki 1996, Francis et al . 2006, López Cabrera & Olivero 2011). Among microfossils, foraminifera are very rare in the LMF.…”
Section: Introductionmentioning
confidence: 99%
“…2a), Telm1 or Valle de las Focas Allomember sensu Marenssi et al . (1998), which is interpreted as early Eocene in age, 52–54 Ma (Marenssi 2006, López Cabrera & Olivero 2011). Fig.…”
Benthic foraminiferal assemblages are described for the first time from the early Eocene of West Antarctica. They come from the lower member (Telm1) of the La Meseta Formation of Isla Marambio (Seymour Island). Two distinctive assemblages, dominated by Nonionellina, Nonionella, Globocassidulina, and Eilohedra, as well as by Globocassidulina, Cribroelphidium, Guttulina, and Lobatula, indicate restricted, shallow marine, nearshore conditions. Their most characteristic species show distinct affinities with Eocene faunas of New Zealand and Patagonia, as well as with stratigraphically younger Antarctic foraminiferal communities.
“…The bryo zoan fauna here com prises 43 spe cies of the dom i nant cerioporine cyc lo stomes along with cheilostomes be long ing to micro poroideans, and umbonulomorph and lepraliomorph ascophorans, where the ma jor ity of col o nies show multilamellar growth. The strata are com posed of poorly con sol i dated sandstones and siltstones, which rep re sent the low er most part of the LMF (Telm1, see Sadler, 1988) or the Valle de las Focas Allomember sensu Marenssi et al (1998), and they are in terpreted to be of Early Eocene age (52-54 Ma; see López-Cabrera and Olivero, 2011).…”
Early to Late Eocene bryo zoans from the La Meseta For ma tion of Sey mour Is land were col lected at two lo cal i ties within the Cucullaea I Allomember (Telm4 and Telm5) on the northwest ern side of the is land and in two lo cal i ties within the Submeseta Allomember (Telm6 and Telm7) on the northeast ern side. This fauna is rep re sented by cyc lo stomes of the suborders Tubuliporina and Cerioporina and suborders of Neocheilostomata, among which nine spe cies have been rec og nized. The fol low ing new spe cies are in tro duced: Micropora nordenskjoeldi sp. nov., Lunulites marambionis sp. nov., Otionellina antarctica sp. nov. and Otionellina eocenica sp. nov. Some other taxa rec og nized in the stud ied ma te rial, such as Reticrescis plicatus, Uharella seymourensis and Celleporaria mesetaensis, were pre vi ously de scribed from the low er most (Telm1) or up per most parts (Telm6-7), thus their strati graphi cal ranges within the La Meseta For ma tion are ex tended. The di verse growth-forms of the bryo zoans in clude a sole ball-shaped celleporiform col ony and re tic u lated and bilamellar-foliaceous colony, as well as rich en crust ing and free-liv ing forms (so-called sand fau nas), in di cat ing the ex is tence of lo cally re stricted shal low-ma rine en vi ron ments. This is par tic u larly true in the mid dle and up per parts of the La Meseta For ma tion (Telm4-7). Re tic u lated, sphe roi dal and ro bust, branched col o nies, which thrived in the en vi ron men tal con di tions of the lower part (Telm1), are rep re sented only by a sparse bryo zoan biota in the up per part of the La Meseta For ma tion. Lunulitiforms, such as Lunulites and Otionellina which are warm wa ter, free-liv ing bryo zoans, dom i nate in the siliciclastic sed i ments of Telm5, but erect folded sheets form ing a shell bed com posed of ?Goodonia oc cur in Telm6-7. These three gen era are rec og nized in Antarctica for the first time. The aus tral ge nus Otionellina has its ear li est fos sil re cord here, show ing close biogeographical links with the Late Eocene-Mio cene fau nas of Aus tra lia and New Zea land. The tax o nomic com po si tion of the stud ied fauna to gether with their growth forms is a very good tool for re con struct ing palaeoenvironmental con di tions in the mid dle and upper parts (Telm4-7) of the La Meseta For ma tion, de pos ited dur ing the Late Ypresian-Priabonian.
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