A Geological Time Scale 2004

Gradstein, Felix M.; Ogg, J G; Smith, Alan G.; Agterberg, F P; Bleeker, Wouter; Cooper, R. A.; Davydov, V; Gibbard, Philip L.; Hinnov, Linda A.; House, M R; Lourens, Lucas Joost; Luterbacher, H -P; McArthur, J; Melchin, M J; Robb, L J; Shergold, J; Villeneuve, M.; Wardlaw, Bruce R.; Ali, J; Brinkhuis, Henk; Hilgen, F J; Hooker, Jerry J.; Howarth, R J; Knoll, Andrew H.; Laskar, Jacques; Monechi, Simonetta; Plumb, K A; Powell, J. H.; Raffi, Isabella; Röhl, Ursula; Sanfilippo, Alessio; Schmitz, B; Shackleton, N J; Shields, G A; Strauß, Harald; Dam, J Van; Kolfschoten, T van; Veizer, J; Wilson, David Gordon

doi:10.4095/215638

Cited by 1,379 publications

(284 citation statements)

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“…2). More recent geological time scales (i.e., Gradstein et al, 2004;Ogg et al, 2008;Gradstein et al, 2012) follow the sequence-stratigraphical interpretation of Hardenbol et al (1998). Small-scale sequences would therefore have lasted around 93 kyr.…”

Section: Sequence and Cyclostratigraphysupporting

confidence: 53%

Timing of sea level, tectonics and climate events during the uppermost Oxfordian (Planula zone) on the Iberian ramp (northeast Spain)

Colombié

Giraud

Schnyder

et al. 2014

Palaeogeography, Palaeoclimatology, Palaeoecology

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The middle Oxfordian warming climate and sea-level rise initiated the development of vast carbonate platforms in some western European basins. At the same time, however, siliciclastics and siliceous sponges dominated certain marginal areas of the Iberian ramp. There, siliciclastic input was particularly prominent during the latest Oxfordian and may have been related to a global sea-level fall, synsedimentary tectonic activity, or humid climatic conditions in the hinterland. Field analyses and computer modeling have been previously used to determine the factors that controlled sedimentation. However, it is still unclear if the specific conditions that prevailed during the latest Oxfordian were due to eustasy, tectonics or climate, and when precisely they occurred. Here, we document major changes in sedimentological, micropalaeontological, and mineralogical records on the Iberian ramp during this interval. Detailed sedimentary facies and palynofacies analyses combined with sequence-stratigraphic and cyclostratigraphic analyses of the Ricla Barranco section enable the establishment of a high-resolution time frame. Based on the quartz and mica percentage fluctuations, one large-and seven small-scale sequences are defined. The large-scale sequence boundaries correlate with third-order sequence boundaries Ox8 and Kim1 defined by Hardenbol et al. (1998). The large-scale maximum-flooding surface corresponds to the base of the most calcareous interval and to the maximum abundance of marine phytoplankton and opaque, equidimensional phytoclasts. The small-scale sequences correspond to the 100-kyr orbital eccentricity cycle. Calcareous nannofossils and clay minerals were used as palaeoclimatic proxies. Nannofossil abundances and fluxes are lower in the upper part than in the lower part of the interval studied, suggesting a decrease in sea-surface trophic conditions, also shown by an increase in the relative abundance of oligotrophic taxa. This upper part is also characterised by an increase in smectite, which coincides with the base of the large-scale highstand deposit, and is interpreted as reflecting the establishment of dry conditions. A first increase in smectite occurs in the lower part of the succession, and coincides with high percentages of quartz and mica. This latter mineralogical assemblage is interpreted as recording the onset of the Late Jurassic to Early Cretaceous rifting stage, which occurred just before the Planula-Galar ammonite Subzone transition. The present study points out a return toward optimum conditions for carbonate sedimentation only 300 kyr after the prominent increase in siliciclastic input due to tectonic activity. The recovery of carbonate production was accompanied by a global sea-level rise and by decreasing rainfall on nearby land.

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Section: Sequence and Cyclostratigraphysupporting

confidence: 53%

Timing of sea level, tectonics and climate events during the uppermost Oxfordian (Planula zone) on the Iberian ramp (northeast Spain)

Colombié

Giraud

Schnyder

et al. 2014

Palaeogeography, Palaeoclimatology, Palaeoecology

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“…Amniote RTT plots were based on the reptile, avian, and mammal chapters of the Fossil Record 2Ј database (4). Here, time intervals were necessarily determined by geological stage boundaries (51). Amniote family origination and extinction rates were estimated as N O /tN t and N E /tN t , respectively (5), where N O and N E are the number of families that respectively originate and disappear during time interval t, and N t is the family diversity at the end of the interval.…”

Section: Detailed Descriptions Of Methods and Results Are Provided Inmentioning

confidence: 99%

Global patterns of diversification in the history of modern amphibians

Roelants

Gower

Wilkinson

et al. 2007

Proc. Natl. Acad. Sci. U.S.A.

586

620

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The fossil record of modern amphibians (frogs, salamanders, and caecilians) provides no evidence for major extinction or radiation episodes throughout most of the Mesozoic and early Tertiary. However, long-term gradual diversification is difficult to reconcile with the sensitivity of present-day amphibian faunas to rapid ecological changes and the incidence of similar environmental perturbations in the past that have been associated with high turnover rates in other land vertebrates. To provide a comprehensive overview of the history of amphibian diversification, we constructed a phylogenetic timetree based on a multigene data set of 3.75 kb for 171 species. Our analyses reveal several episodes of accelerated amphibian diversification, which do not fit models of gradual lineage accumulation. Global turning points in the phylogenetic and ecological diversification occurred after the endPermian mass extinction and in the late Cretaceous. Fluctuations in amphibian diversification show strong temporal correlation with turnover rates in amniotes and the rise of angiosperm-dominated forests. Approximately 86% of modern frog species and >81% of salamander species descended from only five ancestral lineages that produced major radiations in the late Cretaceous and early Tertiary. This proportionally late accumulation of extant lineage diversity contrasts with the long evolutionary history of amphibians but is in line with the Tertiary increase in fossil abundance toward the present. amphibian evolution ͉ macroevolutionary patterns ͉ molecular timetree ͉ paleobiology ͉ phylogenetics P resent-day terrestrial ecosystems harbor Ͼ6,000 amphibian species worldwide (1), a diversity that parallels those of placental mammals and songbirds (2). Yet, the current rate at which amphibian faunas are declining exceeds that of any other vertebrate group and has been attributed to a combination of rapidly changing ecological and climatic conditions (habitat loss, invading pathogens, global warming, increased UV-radiation) (3). This raises questions of how the ancestors of modern amphibians coped with preceding environmental crises during their evolutionary history. The tetrapod fossil record identifies at least one major extinction episode that involved widespread amphibian declines: At the end-Permian [Ϸ251 million years ago (Mya)], a diversity of 24 amphibian-like families (including reptiliomorphs and acanthrosaurs, which may be more related to modern amniotes) was reduced to 8 over a single geological stage boundary (4). The end-Permian mass extinction, estimated to be the most profound loss of vertebrate life on record (4-7), has been associated with a massive release of carbon gases in the atmosphere, causing a global greenhouse effect and abrupt climate warming (6, 7). Similar environmental perturbations have been postulated for subsequent periods and have been associated with fossil evidence for extinctions and subsequent radiations in several amniote groups (8-10). However, there is no correlated pattern for amphibian fossils.T...

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“…Because the COSUNA data cannot easily be placed into Sepkoski's stages for the Lower and Middle Cambrian and because the last interval in the COSUNA data is the Pleistocene, most analyses have been conducted for 71 intervals from the Dresbachian to the Pliocene. Median interval duration is 5.5 million years according to modern stage-boundary age assignments (25).…”

Section: Methodsmentioning

confidence: 99%

Geologic constraints on the macroevolutionary history of marine animals

Peters

2005

Proc. Natl. Acad. Sci. U.S.A.

264

279

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The causes of mass extinctions and the nature of taxonomic radiations are central questions in paleobiology. Several episodes of taxonomic turnover in the fossil record, particularly the major mass extinctions, are generally thought to transcend known biases in the geologic record and are widely interpreted as distinct macroevolutionary phenomena that require unique forcing mechanisms. Here, by using a previously undescribed compilation of the durations of sedimentary rock sequences, I compare the rates of expansion and truncation of preserved marine sedimentary basins to rates of origination and extinction among Phanerozoic marine animal genera. Many features of the highly variable record of taxonomic first and last occurrences in the marine animal fossil record, including the major mass extinctions, the frequency distribution of genus longevities, and short-and long-term patterns of genus diversity, can be predicted on the basis of the temporal continuity and quantity of preserved sedimentary rock. Although these results suggest that geologically mediated sampling biases have distorted macroevolutionary patterns in the fossil record, preservation biases alone cannot easily explain the extent to which the sedimentary record duplicates paleobiological patterns. Instead, these results suggest that the processes responsible for producing variability in the sedimentary rock record, such as plate tectonics and sea-level change, may have been dominant and consistent macroevolutionary forces throughout the Phanerozoic.biodiversity ͉ mass extinction ͉ paleobiology ͉ sedimentary rock ͉ sequence stratigraphy O ne of the most striking aspects of the marine animal fossil record is that it preserves a volatile history of biodiversity and rates of taxonomic origination and extinction. Understanding the causes and evolutionary consequences of this volatility is one of the central goals of paleobiology. It has long been recognized, however, that the quantity of preserved sedimentary rock varies over short and long intervals of geologic time (1-3) and that this variation is correlated with several important macroevolutionary patterns in the fossil record, including changes in biodiversity (4-8) and rates of taxonomic extinction (4, 9, 10). The mutual correlations between preserved rock quantity and macroevolutionary patterns have been interpreted as evidence for either preservation biases that distort the apparent timings of extinction and origination in the fossil record (bias hypothesis) (4-7, 10) or a common pattern that is induced by processes, such as sea level fluctuations, plate tectonics, and resultant changes in marine shelf area, that affect both the amount of preserved rock and biological evolution (commoncause hypothesis) (6, 7, 9-12). Nevertheless, some workers have proffered that many intervals of turnover in the fossil record, particularly the major mass extinctions (13), are too substantial to be the result of preservation biases and are sufficiently distinct to require unique forcing mechanisms (14-17).Evaluati...

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A Geological Time Scale 2004

Cited by 1,379 publications

References 0 publications

Timing of sea level, tectonics and climate events during the uppermost Oxfordian (Planula zone) on the Iberian ramp (northeast Spain)

Timing of sea level, tectonics and climate events during the uppermost Oxfordian (Planula zone) on the Iberian ramp (northeast Spain)

Global patterns of diversification in the history of modern amphibians

Geologic constraints on the macroevolutionary history of marine animals

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