Advances in sequence stratigraphy and the development of depositional models have helped explain the origin of genetically related sedimentary packages during sea level cycles. These concepts have provided the basis for the recognition of sea level events in subsurface data and in outcrops of marine sediments around the world. Knowledge of these events has led to a new generation of Mesozoic and Cenozoic global cycle charts that chronicle the history of sea level fluctuations during the past 250 million years in greater detail than was possible from seismic-stratigraphic data alone. An effort has been made to develop a realistic and accurate time scale and widely applicable chronostratigraphy and to integrate depositional sequences documented in public domain outcrop sections from various basins with this chronostratigraphic framework. A description of this approach and an account of the results, illustrated by sea level cycle charts of the Cenozoic, Cretaceous, Jurassic, and Triassic intervals, are presented.

https://science.sciencemag.org/content/sci/235/4793/1156.full.pdf

Chronology of fluctuating sea levels since the triassic.

The role of fossils in dating the tree of life has been misunderstood. Fossils can provide good "minimum" age estimates for branches in the tree, but "maximum" constraints on those ages are poorer. Current debates about which are the "best" fossil dates for calibration move to consideration of the most appropriate constraints on the ages of tree nodes. Because fossil-based dates are constraints, and because molecular evolution is not perfectly clock-like, analysts should use more rather than fewer dates, but there has to be a balance between many genes and few dates versus many dates and few genes. We provide "hard" minimum and "soft" maximum age constraints for 30 divergences among key genome model organisms; these should contribute to better understanding of the dating of the animal tree of life.

/pdf/paleontological-evidence-to-date-the-tree-of-life-5dhwbwgnyr.pdf

Paleontological Evidence to Date the Tree of Life

The extensive work carried out during more than a decade by the International Subcommission on Ordovician Stratigraphy has resulted in a new global classification of the Ordovician System into three series and seven stages. Formal Global Boundary Stratotype Section and Points (GSSPs) for all stages have been selected and these and the new stage names have been ratified by the International Commission on Stratigraphy. Based on a variety of biostratigraphic data, these new units are correlated with chronostratigraphic series and stages in the standard regional classifications used in the UK, North America, Baltoscandia, Australia, China, Siberia and the Mediterranean-North Gondwana region. Furthermore, based mainly on graptolite and conodont zones, the Ordovician is subdivided into 20 stage slices (SS) that have potential for precise correlations in both carbonate and shale facies. The new chronostratigraphic scheme is also tied to a new composite δ13C curve through the entire Ordovician.

The new chronostratigraphic classification of the Ordovician System and its relations to major regional series and stages and to δ13C chemostratigraphy

In post-Cambrian time, five events—the end-Ordovician, end-Frasnian in the Late De- vonian, end-Permian, end-Triassic, and end-Cretaceous—are commonly grouped as the ''big five'' global intervals of mass extinction. Plotted by magnitude, extinction intensities for all Phanerozoic substages show a continuous distribution, with the five traditionally recognized mass extinctions located in the upper tail. Plotted by time, however, proportional extinctions clearly divide the Phan- erozoic Eon into six stratigraphically coherent intervals of alternating high and low extinction in- tensity. These stratigraphic neighborhoods provide a temporal context for evaluating the intensity of extinction during the ''big five'' events. Compared with other stages and substages in the same neighborhood, only the end-Ordovician, end-Permian, and end-Cretaceous extinction intensities appear as outliers. Moreover, when origination and extinction are considered together, only these three of the ''big five'' events appear to have been generated exclusively by elevated extinction. Low origination contributed more than high extinction to the marked loss of diversity in the late Fras- nian and at the end of the Triassic. Therefore, whereas the ''big five'' events are clearly times when diversity suffered mass depletion, only those at the end of the Ordovician, Permian, and Cretaceous periods unequivocally qualify as globally distinct mass extinctions. Each of the three has a unique pattern of extinction, and the diversity dynamics of these events differ, as well, from the other two major diversity depletions. As mass depletions of diversity have no common effect, common cau- sation seems unlikely.

/pdf/origination-extinction-and-mass-depletions-of-marine-xm1c0ctwn2.pdf

Origination, Extinction, and Mass Depletions of Marine Diversity

▪ Abstract Near the end of the Late Ordovician, in the first of five mass extinctions in the Phanerozoic, about 85% of marine species died. The cause was a brief glacial interval that produced two pulses of extinction. The first pulse was at the beginning of the glaciation, when sea-level decline drained epicontinental seaways, produced a harsh climate in low and mid-latitudes, and initiated active, deep-oceanic currents that aerated the deep oceans and brought nutrients and possibly toxic material up from oceanic depths. Following that initial pulse of extinction, surviving faunas adapted to the new ecologic setting. The glaciation ended suddenly, and as sea level rose, the climate moderated, and oceanic circulation stagnated, another pulse of extinction occurred. The second extinction marked the end of a long interval of ecologic stasis (an Ecologic-Evolutionary Unit). Recovery from the event took several million years, but the resulting fauna had ecologic patterns similar to the fauna that had become e...

The Late Ordovician Mass Extinction

At its 1969 meeting, The Pander Society convened a symposium on conodont biostratigraphy that resulted in a volume (Sweet & Bergstrom 1971a) in which specialists systematically summarized the status of conodont-based biostratigraphy up to 1969. One function of such a volume is to direct attention to areas that need more work and to focus on conclusions in need of more robust verification. The Pander Society's biostratigraphy volume provides this focus and has also been a very useful guide to the biostratigraphic uses of conodonts. In the 14 years since the volume appeared, additional effort has been expended on then-tentative biostratigraphic schemes, and revised or alternative biostratigraphic scales have been stimulated for several intervals. We cannot hope in this review to bring the Pander Society's bio­ stratigraphy volume fully up to date, or even to review all major lines of progress in conodont-based biostratigraphy of the past 14 years. What we can do is note major changes offairly recent vintage, with emphasis on areas in which the application of different correlation algorithms has confirmed systems that were apparently well established in 1971, or in which use of different correlation methodology has resulted in a different view of these systems. Our discussion deals largely with Ordovician and Triassic biostratigraphy, our areas of expertise, and with the contrast in those areas between the results of traditional biozonal practices and those of less conventional graphic procedures.

Conodonts and biostratigraphic correlation

Ceratitic ammonoids from the Greville Formation in the Nelson Regional Syncline, South Island of New Zealand, were described as a new genus and species of the Ophiceratidae, Durvilleoceras woodmani, and dated as ‘late Middle Permian’ (Waterhouse, 1973). In fact, Durvilleoceras differs from all known Permian ammonoids in both conch form and sutural pattern, but closely resembles lower Triassic ceratites. Structural and sedimentologic complexities within the Nelson Syncline are such that stratigraphic interpretations are questionable, and the fauna of both the Greville and adjacent formations is sparse. Consequently, we consider that Durvilleoceras is best interpreted as a middle Scythian ceratite of the family Flemingitidae.

Reinterpretation of ceratitic ammonoids from the Greville Formation, New Zealand

Muscle-attachment impressions are described for the first time from representatives of the nautiloid suborders Oncoceratina (Oncoceras sp., Beloitoceras sp., Diestoceras sp.) Ascoceratina (Billingsites deformis (Eichwald)?, Discosorina (Parryoceras euchari Sweet & Miller), and Rutoceratina (Metacoceras sp.). Notes concerning the probable configuration of such impressions in certain Paleozoic Barrandeoceratina (Charactoceras?) and Triassic Lyroceratina (Proclydonautilus ursensis Smith) are included. Muscle-attachment impressions are not known in the Endoceratina and Actinoceratina; in known Ellesmeroceratina, Michelinoceratina, and secondarily straight Tarphyceratina (Lituitidae) the retractors were attached dorsally ("dorsomyarian"), whereas in described Barrandeoceratina, coiled Tarphyceratina, Ascoceratina, Oncoceratina, and Discosorina, these muscles were attached ventrally ("ventromyarian"). Described Rutoceratina, Nautilina, Solenochilina, and Lyroceratina are similar in that the retractors were attached laterally ("pleuromyarian"). In several cases, similar attachment patterns suggest adaptive convergence, rather than relationship, and their taxonomic significance is thereby reduced.

Muscle-attachment impressions in some Paleozoic nautiloid cephalopods

Eighteen previously described conodont species distributed among 11 genera are described from the Nowshera reef limestones of the northern part of West Pakistan. The identified species are lowermost Devonian and are equivalent in part to the western European Spathognathodus oesteinhornensis and Icriodus woschmidti zones.

Conodonts from Nowshera reef limestones (uppermost Silurian or lowermost Devonian), West Pakistan

The Fairview and McMillan formations of the Cincinnati region, the reference standard for the North American Maysville stage (Upper Ordovician), have yielded a large collection of conodont elements, referable to 29 species, distributed among 18 genera. Fourteen species are known to range through the Eden, Fairview, and McMillan formations; most of these are represented as well in late Mohawkian and Trentonian strata in the midcontinent province of North America, and several continue into the Richmond group. Three species in the Fairview fauna occur also in the Eden, but do not range above the Fairview locally; 7 species are restricted to the Fairview. Four species, introduced locally in late Eden or early Fairview strata, continue into the McMillan, which otherwise contains a reduced fauna of long-ranging midcontinent species. The presence of Ambalodus, Amorphognathus, and Belodina in Eden and Fairview strata, but not above them, suggests that the Orchard Creek shale of Missouri, the pre-upper Brainard Maquoketa shale of Iowa, and the Maravillas formation of Texas (which have all yielded representatives of these genera) are Maysville in age, or older. Four species (Eoligonodina fairmountensis, Oulodus casteri, Prioniodina velicuspis, and Zygognathus maysvillensis) are described for the first time.

Walter C. Sweet

Papers

Conodonts and biostratigraphic correlation

Reinterpretation of ceratitic ammonoids from the Greville Formation, New Zealand

Muscle-attachment impressions in some Paleozoic nautiloid cephalopods

Conodonts from Nowshera reef limestones (uppermost Silurian or lowermost Devonian), West Pakistan

The American Upper Ordovician standard, [Part] 3, Conodonts from the Fairview and McMillan formations of Ohio, Kentucky and Indiana