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32 results for “late Paleozoic”
Global kinematics of tectonic plates and subduction zones since the late Paleozoic Era
<div>Global kinematics of tectonic plates and subduction zones since the late Paleozoic Era</div> <div> </div> <div>Alexander Young(1), Nicolas Flament(1), Kayla Maloney(2), Simon Williams(2), Kara Matthews(2), Sabin Zahirovic(2), Dietmar Müller(2,3)</div> <div> </div> <div>1. The University of Wollongong, NSW 2522, Australia </div> <div> </div> <div>2. EarthByte Group, School of Geosciences, The University of Sydney, NSW 2006, Australia</div> <div> </div> <div>3. Sydney Informatics Hub, The University of Sydney, NSW 2006, Australia </div> <div> </div> <div>Contact: ajy321@uowmail.edu.au</div> <div> </div> <div> </div> <div>Supplementary Material</div> <div> </div> <div>We provide the digital plate model files (including rotations and geometries). These files allow for the visualisation and/or manipulation of the late Paleozoic to present-day (410-0 Ma) global plate motion model presented in this study. </div> <div> </div> <div>#########################################</div> <div>The digital plate model files are compatible with the open-source GPlates plate reconstruction software (<a href="https://www.gplates.org" target="_blank" rel="noopener">www.gplates.org</a>):</div> <div> </div> <div>(1) Rotations - Global rotation model that contains the reconstruction poles that describe the motions of the continents and oceans.</div> <div>- <strong>Global_250-0Ma_Young_et_al.rot</strong> (455 KB)</div> <div>-<strong> Global_410-250Ma_Young_et_al.rot</strong> (154 KB)</div> <div> </div> <div>(2) Plate polygons and boundary geometries - Topologically closed plate polygons are constructed from the intersection of ridges, transforms, subduction zones and other plate boundary geometries. These 'resolved topologies' are defined at 1 Myr intervals (410-0 Ma). The plate boundary geometries and plate polygons have been assigned plate reconstruction IDs to allow them to be reconstructed using the supplied rotation file.</div> <div>- <strong>Global_Mesozoic-Cenozoic_plate_bounds_Young_etal.gpml</strong> (36.5 MB)</div> <div>- <strong>Global_Paleozoic_plate_bounds_Young_etal.gpml</strong> (6.7 MB)</div> <div>- <strong>TopologyBuildingBlocks_Young_etal.gpml</strong> (2 MB) - this file is identical to Müller et al. (2016)</div> <div> </div> <div>(3) Coastlines - Geometries of the present-day coastlines.</div> <div>- <strong>Global_coastlines_Young_et_al_low_res.shp</strong> (1.2 MB including auxiliary files, datum-WGS 1984)</div> <div> </div> <div>(4) Static polygons (optional) - Includes ocean isochron and terrane polygon geometries.</div> <div>- <strong>GlobalPresentDay_SPP_Young_etal.shp</strong> (1.4 MB inc. auxillary files, datum-WGS 1984)</div> <div> </div> <div>(5) Continental polygons (optional) - Includes continental terrane polygon geometries and excludes oceanic lithosphere.</div> <div>- <strong>PresentDay_ContPolygons_Young_etal.shp</strong> (451 KB inc. auxillary files, datum-WGS 1984)</div> <div> </div> <div>GPlates: </div> <div>To view the model, load all files in GPlates (either drag and drop files onto the globe OR from the navigation bar at the top of the screen click File -> Open Feature Collection and select files). Both rotation files (1) and each of the three plate geometry files (2) need to be loaded for the model to work properly. It is recommended that coastlines (3) are loaded to see how the continents move, however only one coastline file is necessary (.gpml or .shp). The static polygons (4) and continental polygons (5) are optional. </div> <div> </div> <div>The two rotation files need to be 'connected' in order for the model to run continuously from 410 to 0 Ma. In the GPlates 'Layers' window (opened from the main navigation bar, click 'Window' -> 'Show Layers') the rotation files will be highlighted yellow, yet only one will have a yellow tick next to it to signify it is being used. Click the small black triangle to the left the ticked rotation file. Under 'Inputs' -> 'Reconstruction features' click 'Add new connection' and then select the other rotation file from the list of files that will appear. This will ensure that both rotation files are active. </div> <div> </div> <div>Finally, it is recommended to experiment with geometry visibility in order to make the globe less cluttered. For instance, from the navigation bar click View -> Geometry Visibility and untick 'Show Line Geometries'. Alternatively, files can be toggled on and off using the tick boxes in the Layers window. For more information about using GPlates, a set of user tutorials can be accessed from the GPlates website - http://www.gplates.org/docs.html.</div> <div> </div> <div> </div> <div>#########################################</div> <div>MODEL REFERENCING:</div> <div>When using our model, in addition to citing this publication, please consider citing the studies of Domeier and Torsvik (2014), Matthews et al. (2016) and Müller et al. (2016) which served as the basis for this model in the late Paleozoic and Mesozoic-Cenozoic, respectively, and citing any other study that describes refinements to the plate reconstructions in your region of interest as appropriate. </div> <div> </div> <div>- Domeier, M., & Torsvik, T. H. (2014). Plate tectonics in the late Paleozoic. Geoscience Frontiers, 5(3), 303-350. DOI: <a href="https://doi.org/10.1016/j.gsf.2014.01.002" target="_blank" rel="noopener">10.1016/j.gsf.2014.01.002</a></div> <div>- Müller, R. D., Seton, M., Zahirovic, S., Williams, S. E., Matthews, K. J., Wright, N. M., Shephard, G. E., Maloney, K., Barnett-Moore, N., Hosseinpour, M., Bower, D. J., & Cannon, J. (2016). Ocean Basin Evolution and Global-Scale Plate Reorganization Events Since Pangea Breakup. Annual Review of Earth and Planetary Sciences, 44(1). DOI: <a href="https://doi.org/10.1146/annurev-earth-060115-012211" target="_blank" rel="noopener">10.1146/annurev-earth-060115-012211</a></div> <div>-Matthews, K. J., Maloney, K. T., Zahirovic, S., Williams, S. E., Seton, M., & Mueller, R. D. (2016). Global plate boundary evolution and kinematics since the late Paleozoic. Global and Planetary Change, 146, 226-250.</div> <div>DOI: <a href="https://doi.org/10.1016/j.gloplacha.2016.10.002" target="_blank" rel="noopener">10.1016/j.gloplacha.2016.10.002</a></div>
Global plate boundary evolution and kinematics since the late Paleozoic
<h3>Global plate boundary evolution and kinematics since the late Paleozoic </h3> <p>Kara J. Matthews*^, Kayla T. Maloney*, Sabin Zahirovic*, Simon E. Williams*, Maria Seton*, R. Dietmar Müller*</p> <p>* EarthByte Group, School of Geosciences, The University of Sydney, Sydney, NSW 2006, Australia<br>^ Present address: Department of Earth Sciences, University of Oxford, South Parks Road, Oxford OX1 3AN, UK</p> <p>Contact: karajmatthews@gmail.com</p> <p>CORRECTION applied for the Pacific plate prior to 83 Ma based on Torsvik et al. (2019)</p> <h3><br>Supplementary Material</h3> <p>We provide a digital plate model files (including rotations and geometries) with this publication. These files allow for the visualisation and/or manipulation of the late Paleozoic to present-day (410-0 Ma) global plate motion model presented in this study. </p> <p>#########################################<br>The digital plate model files are compatible with the open-source GPlates plate reconstruction software (<a href="https://www.gplates.org" target="_blank" rel="noopener">www.gplates.org</a>):</p> <p>(1) Rotations - Global rotation model that contains the reconstruction poles that describe the motions of the continents and oceans.<br>- <strong>Global_EB_250-0Ma_GK07_Matthews_etal.rot</strong> (455 KB)<br>- <strong>Global_EB_410-250Ma_GK07_Matthews_etal.rot</strong> (115 KB) - in the comments 'POLE_RECALCULATED' means that we recalculated that finite pole of rotation such that the moving plate moves relative to a neighbouring plate rather than directly to the absolute reference frame (see Section 2.2.1 of the main text for more details). This process should have a minimal effect on the absolute motion of the plate.</p> <p>(2) Plate polygons and boundary geometries - Topologically closed plate polygons are constructed from the intersection of ridges, transforms, subduction zones and other plate boundary geometries. These 'resolved topologies' are valid at 1 Myr intervals (410-0 Ma). The plate boundary geometries and plate polygons have been assigned plate reconstruction IDs to allow them to be reconstructed using the supplied rotation file.<br>- <strong>Global_Mesozoic-Cenozoic_plate_bounds_Matthews_etal.gpml</strong> (36 MB)<br>- <strong>Global_Paleozoic_plate_bounds_Matthews_etal.gpml</strong> (8.7 MB)<br>- <strong>TopologyBuildingBlocks_Matthews_etal.gpml</strong> (2 MB) - this file has not been modified from Müller et al. (2016)</p> <p>(3) Coastlines - Geometries of the present-day coastlines.<br>- <strong>Global_coastlines_low_res_Matthews_etal.gpml</strong> (25.4 MB)<br>- <strong>Global_coastlines_low_res_Matthews_etal.shp</strong> (2.9 MB inc. auxillary files, datum-WGS 1984)<br>NOTE: From 410 to 320-310 Ma Kazakhstania is represented as one or two ('Internal' and 'External' Kazakhstania - Domeier and Torsvik, 2014) ovate polygons. Kazakhstania is highly deformed following a long and complicated history, and so for simplicity we avoid using their present-day outlines in the earlier part of the model.</p> <p>(4) Static polygons (optional) - Includes ocean isochron and terrane polygon geometries.<br>- <strong>Global_EarthByte_GPlates_PresentDay_StaticPlatePolygons_Matthews_etal.shp</strong> (2.7 MB inc. auxillary files, datum-WGS 1984)</p> <p>(5) Continenal polygons (optional) - Includes continental terrane polygon geometries and excludes oceanic lithosphere.<br>- <strong>Global_EarthByte_GPlates_PresentDay_ContinentalPolygons_Matthews_etal.shp</strong> (804 KB inc. auxillary files, datum-WGS 1984)</p> <p>GPLATES: <br>To view the model load all files in GPlates (either drag and drop files onto the globe OR from the navigation bar at the top of the screen click File -> Open Feature Collection and select files). Both rotation files (1) and each of the three plate geometry files (2) need to be loaded for the model to work properly. It is recommended that coastlines (3) are loaded to see how the continents move, however only one coastline file is necessary (.gpml or .shp). The static polygons (4) and continental polygons (5) are optional. </p> <p>The two rotation files need to be 'connected' in order for the model to run continuously from 410 to 0 Ma. In the GPlates 'Layers' window (opened from the main navigation bar, click 'Window' -> 'Show Layers') the rotation files will be highlighted yellow, yet only one will have a yellow tick next to it to signify it is being used. Click the small black triangle to the left the ticked rotation file. Under 'Inputs' -> 'Reconstruction features' click 'Add new connection' and then select the other rotation file from the list of files that will appear. This will ensure that both rotation files are active. </p> <p>Finally, it is recommended to experiment with geometry visibility in order to make the globe less cluttered. For instance, from the navigation bar click View -> Geometry Visibility and untick 'Show Line Geometries'. Alternatively, files can be toggled on and off using the tick boxes in the Layers window. For more information about using GPlates, a set of user tutorials can be accessed from the GPlates website - http://www.gplates.org/docs.html.</p> <p><br>#########################################<br>We also provide a list of the plate reconstruction IDs used in the model:</p> <p>Plate IDs - A list of all the plate IDs used in the rotation and geometry files and their corresponding plate names.<br>- <strong>EarthByte_Plate_ID_Table_Matthews_etal.txt</strong> (33 KB)</p> <p>#########################################<br>MODEL REFERENCING:<br>When using our model, in addition to citing this publication:</p> <p>Matthews, K.J., Maloney, K.T., Zahirovic, S., Williams, S.E., Seton, M. and Müller, R.D., 2016, Global plate boundary evolution and kinematics since the late Paleozoic, Global and Planetary Change, in press, accepted 3 October 2016.</p> <p>please also consider citing the studies of Domeier and Torsvik (2014) and Müller et al. (2016) which served as the basis for this model in the late Paleozoic and Mesozoic-Cenozoic, respectively, and cite any other study that describes refinements to the plate reconstructions in your region of interest. See Section 2 and Section 3 of the main text for more information on how the present model was constructed.</p> <p>- Domeier, M., & Torsvik, T. H. (2014). Plate tectonics in the late Paleozoic. Geoscience Frontiers, 5(3), 303-350. DOI:<a href="https://doi.org/10.1016/j.gsf.2014.01.002" target="_blank" rel="noopener">10.1016/j.gsf.2014.01.002</a><br>- Müller, R. D., Seton, M., Zahirovic, S., Williams, S. E., Matthews, K. J., Wright, N. M., Shephard, G. E., Maloney, K., Barnett-Moore, N., Hosseinpour, M., Bower, D. J., & Cannon, J. (2016). Ocean Basin Evolution and Global-Scale Plate Reorganization Events Since Pangea Breakup. Annual Review of Earth and Planetary Sciences, 44(1). DOI:<a href="https://doi.org/10.1146/annurev-earth-060115-012211" target="_blank" rel="noopener">10.1146/annurev-earth-060115-012211</a></p> <p>Note: We have recently fixed some issues in this model, namely the motion of the Pacific plate (following Torsvik et al., 2019), and some MOR topologies in the Arctic. The fixes are in the model files included in this folder, but the old (published) version of the model is included in a sub-folder called "_OLD_MODEL_DO_NOT_USE". </p> <p>Torsvik, T. H., B. Steinberger, G. E. Shephard, P. V. Doubrovine, C. Gaina, M. Domeier, C. P. Conrad, and W. W. Sager (2019), Pacific‐Panthalassic reconstructions: Overview, errata and the way forward, Geochemistry, Geophysics, Geosystems, 20(7), 3659-3689.</p> <p> </p>
FIGURE 2 in Biodiversity patterns across the Late Paleozoic Ice Age
FIGURE 2. Turnover rates during the LPIA with clades plotted individually and merged. Mean sea-surface temperature (SST) after Song et al. (2019). The two main phases of the glaciation indicated with snowflakes.
Figure 9 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 9. Phylogenetic relationships within Eryopidae as found in the present analysis, with the most important synapomorphies mapped onto nodes. See Appendix A for character definitions and a matrix, and see the text for a complete list of results.
Figure 8 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 8. Morphometrics of eryopiform skulls, depicting crucial skull proportions relative to size. Arrows in (a) highlight ontogeny in O. labyrinthicus and S. haeuseri.
Figure 6 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 6. Cranial morphology in eryopid temnospondyls, exemplified by reconstructed skull dorsal views. (a) Actinodon frossardi (after Werneburg, 1997), (b) Osteophorus roemeri (after Meyer, 1860), (c) Glaukerpeton avinoffi (after Werneburg and Berman, 2012), (d) Onchiodon labyrinthicus (after Boy, 1990), (e) Onchiodon thuringiensis (after Werneburg, 2008), (f) Clamorosaurus nocturnus (after Gubin, 1983, and photographs courteously provided by Ralf Werneburg), (g) Eryops sp. from the Moran Formation (MCZ 1914), (h) Eryops anatinus (AMNH 4310), (i) Eryops megacephalus (MCZ 1129). Darker shading figures depressions on the dorsal side of the skull roof.
Figure 7 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 7. Morphospace occupation of eryopiform skulls, showing differences in ontogenetic change and morphometric variance between Onchiodon labyrinthicus and Sclerocephalus spp. and adult skulls of other eryopids. (a) PC1–PC2 axes, (b) areas occupied by immature Onchiodon and Sclerocephalus compared, (c) close-up of (a) with focus on variation in O. labyrinthicus, and (d) PC1 plotted against size.
Figure 2 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 2. Larger juveniles of Onchiodon labyrinthicus Geinitz. (a) LFUG 13570, (b) LFUG 13501, (c) MMG SaP 356, (d) LFUG 13391, (e) LFUG 13398, (f) LFUG 13609, (g) LFUG 13047. Darker shading figures depressions on the dorsal side of the skull roof. Scale equals 10 mm.
Figure 4 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 4. Reconstruction of skulls in dorsal view Onchiodon labyrinthicus Geinitz. (a) MMG SaP 237, (b) LFUG 13343, (c) LFUG 13405, (d) MMG SaP 356, (e) LFUG 13391, (f) LFUG 13570, (g) LFUG 13501, (h) LFUG 13292. Darker shading figures depressions on dorsal side of skull roof. Scale equals 10 mm.
Figure 5 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 5. Palate of Onchiodon labyrinthicus Geinitz, in ventral view. (a) LFUG 13394, (b) LFUG 13514. Darker grey is the inner side of the skull roof. Scale equals 10 mm.
Figure 3 in The life cycle in late Paleozoic eryopid temnospondyls: developmental variation, plasticity and phylogeny
Figure 3. Ontogeny of the dermal ornament in Onchiodon labyrinthicus Geinitz. (a) LFUG 13343, (b) MMG SaP 390, (c) MMG SaP 356, (d) MMG SaP 361, (e) LFUG 13395, (f) LFUG 13391, (g) LFUG 13570, (h) LFUG 13292.
Resolving the tectonic setting of South China in the late Paleozoic
<p><span><span>The tectonic setting of South China during the late Paleozoic is essential to understanding the geodynamics off the eastern margin of Pangea supercontinent due to its unique paleo-position at the confluence of the Paleo-Tethys and Panthalassic oceans. </span>Here, we present integrated biostratigraphic, geochronological, and isotope geochemical data on the late Carboniferous siliciclastic rocks from southeast South China in order to decipher the tectonic evolution of the South China Block. We collected three siliciclastic samples from the section at stratigraphic heights of 0.6 m, 16 m, and 26 m. The U-Pb age dating of detrital zircons was conducted by LA-ICP-MS at the Tianjin Center of Geological Survey. </span>Glass NIST 610 was used as external standards for trace element calibration. Zircon Hf isotopic data were conducted by LA-MC-ICP-MS at Nanjing FocuMS Technology Co. Ltd. We also compiled zircon U-Pb age data and Hf isotopic d<span>ata from previously published sources, including Hu et al. 2015, Hu et al. 2012, Li et al. 2020, 2017 and Li et al. 2012.</span></p>
Resolving the tectonic setting of South China in the late Paleozoic
Open the record for dataset details and reuse information.
Grain-size control on detrital zircon cycloprovenance in the late Paleozoic Paradox and Eagle basins, USA
<p>Detrital zircon U-Pb and grain size data for JGR: Solid Earth: "Grain size control on detrital zircon cycloprovenance in the late Paleozoic Paradox and Eagle basins, USA" by Ryan J. Leary, M. Elliot Smith, and Paul Umhoefer. </p>
Data from: Heterochronic origin of spherical fusulinid foraminifera in the Late Paleozoic
<p><span>Heterochrony describes acceleration, displacement and/or retardation of descendants' development events compared to ancestral states and has often been cited as an important process to bring about morphological novelty. It was coined one and half centuries ago and has been discussed by both paleobiologists and biologists frequently ever since. Many types of fossil organisms preserve aspects of their development histories in their bones or shells that have been used for heterochrony analyses, with body size being used as a developmental age indicator, despite raised questions regarding this practice. For organisms whose hard structures consist of multiple chambers, or that contain growth lines, age information suggested by these structures independently can facilitate ontogenetic modeling. In this way, relations among size, shape and age can be established in order to document patterns of morphological development.</span></p> <p><span>Morphological analysis of pseudoschwagerine fusulinids, a fossil foraminifera group that developed a morphologically novel spherical shell, along with their presumptive triticitid ancestors illustrates this approach to heterochrony analysis. Ontogenetic trajectory comparisons of four major pseudoschwagerine genera, as well as those of triticitid foraminifera, document relations between their shape, size and developmental ages. A complex of heterochronic patterns including peramorphic pre-displacement, hypermorphosis and acceleration characterize pseudoschwagerine development and appear to be responsible for the novel appearance of large, inflated fusiform and spherical tests in these Late Paleozoic benthic foraminifera. The morphometric approach employed in this investigation could be applied widely in the quantitative morphological studies of development histories in a variety of other fossil groups. </span></p>
Data from: Local and global abundance associated with extinction risk in late Paleozoic and early Mesozoic gastropods
Ecological theory predicts an inverse association between population size and extinction risk, but most previous paleontological studies have not confirmed this relationship. The reasons for this discrepancy between theory and observation remain poorly understood. In this study, we compiled a global database of gastropod occurrences and collection-level abundances spanning the Early Permian through Early Jurassic (Pliensbachian). Globally, the database contains 5469 occurrences of 496 genera and 2156 species from 839 localities. Within the database, 30 collections distributed across 7 stages contain at least 75 specimens and 10 genera – our minimum criteria for within-collection analysis of extinction selectivity. We use logistic regression analysis to assess the relationship between abundance and extinction risk using global and local measures of population size and stage-level extinction patterns in Early Permian through Early Jurassic marine gastropods. We find that global genus occurrence frequency is inversely associated with extinction risk (i.e., positively associated with survival) in 15 of 16 stages examined, statistically significantly so in 6 stages. Although correlation between geographic range and occurrence frequency may account for some of this association, results from multivariable regression analysis suggest that the association between occurrence frequency and extinction risk is largely independent of geographic range. Within local assemblages, abundance (number of individuals) is also inversely associated with extinction risk. The strength of association is consistent across time and modes of fossil preservation. Effect strength is poorly constrained, particularly in analyses of local collections. In addition to limited power due to small sample size, this poor constraint may result from confounding by ecological variables not controlled for in the analyses, by taphonomic or collection biases, or from non-monotonic relationships between abundance and extinction risk. Two factors are likely to account for the difference between our results and those of most previous studies. First, many previous studies focused on the end-Cretaceous mass extinction event; the extent to which these results can be generalized to other intervals remains unclear. Second, previous findings of non-selective extinction could result from insufficient statistical power rather than the absence of an underlying effect because non-selective extinction is generally used as the null hypothesis for statistical convenience. Survivorship patterns in late Paleozoic and early Mesozoic gastropods suggest that abundance has been a more important influence on extinction risk through the Phanerozoic than previously appreciated.
Data from: Late Paleozoic fusulinoidean gigantism driven by atmospheric hyperoxia
Atmospheric hyperoxia, with pO2 in excess of 30%, has long been hypothesized to account for late Paleozoic (360-250 million years ago) gigantism in numerous higher taxa. However, this hypothesis has not been evaluated statistically because comprehensive size data have not been compiled previously at sufficient temporal resolution to permit quantitative analysis. In this study, we test the hyperoxia-gigantism hypothesis by examining the fossil record of fusulinoidean foraminifers, a dramatic example of protistan gigantism with some individuals exceeding 10 cm in length and exceeding their relatives by six orders of magnitude in biovolume. We assembled and examined comprehensive regional and global, species-level datasets containing 270 and 1823 species, respectively. A statistical model of size evolution forced by atmospheric pO2 is conclusively favored over alternative models based on random walks or a constant tendency toward size increase. Moreover, the ratios of volume to surface area in the largest fusulinoideans are consistent in magnitude and trend with a mathematical model based on oxygen transport limitation. We further validate the hyperoxia-gigantism model through an examination of modern foraminiferal species living along a measured gradient in oxygen concentration. These findings provide the first quantitative confirmation of a direct connection between Paleozoic gigantism and atmospheric hyperoxia.
Data from: Compositional turnover and ecological changes related to the waxing and waning of glaciers during the Late Paleozoic ice age in ice-proximal regions (Pennsylvanian, western Argentina)
The late Paleozoic ice age (LPIA) had a profound effect on the biota. Despite much research having been focused on paleotropical regions or global-scale analyses, regional ecological changes have seldom been studied in ice-proximal basins. Here, I study the compositional turnover and diversity structure across the main Carboniferous glacial event recorded in western Argentina and the subsequent nonglacial interval. Brachiopod and bivalve data from western Argentina suggest that the transition from glacial to nonglacial climates caused major compositional changes. Turnover, however, was not uniform across the bathymetric gradient, being higher in deep environments. Because extirpation was concentrated in brachiopods, but immigration was similar in both clades, the taxonomic structure of the region was significantly modified. Although regional hierarchical diversity structure and occupancy distributions remained stable, dissecting the analysis in brachiopods and bivalves underscores that both clades had different responses to climate change. Brachiopods, on the one hand, show stability in the diversity structure and a very slight decrease in occupancies of intermediate genera, while bivalves show an important rise in diversity, both at the environment and regional scale, and an increase in genera with intermediate occupancies. The bathymetric diversity gradient was also modified from hump shaped with maximum diversity in the deep subtidal to a linear gradient with maximum values toward the offshore. However, relative compositional differences within environments remained stable, with maximum values at intermediate depths both in glacial and nonglacial intervals. Moreover, local-scale coexistence between brachiopods and bivalves changed in the nonglacial interval, showing significant segregation, which indicates relevant modifications in community assembly dynamics. Results from western Argentina highlight the magnitude of regional-scale ecological changes during the LPIA in ice-proximal regions, suggesting that the waxing and waning of glaciers was able to cause regional taxonomic turnover and medium-scale ecological changes even during intervals of relative macroevolutionary quiescence.
Data of "Revisiting the Late Paleozoic–Mesozoic tectonic evolution of epicontinental eastern Central Asian Orogenic Belt on the basis of detrital zircon"
<p><strong>Ds01.</strong> Table S1. Zircon U–Pb isotopic and trace element data of mica-quartz schist (14JH12-1) from the Hulin Basin.</p> <p><strong>Ds02. </strong>Table S2. Zircon U–Pb isotopic and trace element data of fine sandstone (JHD53) from the Wandashan accretionary complex.</p> <p><strong>Ds03.</strong> Table S3. Zircon U–Pb isotopic and trace element data of sandy slate (JHD44) from the Wandashan accretionary complex.</p> <p><strong>Ds04.</strong> Table S4. Collected sedimentary rock samples and our samples in NE China, showing their original and renamed sample ID and dating data.</p>
Paleomagnetism of the Middle and Late Permian rocks from eastern Tibet constrains the Late Paleozoic paleography and drift history of the North Qiangtang terrane
<p>The Qinghai-Tibet Plateau comprises a mosaic of geologically distinct Paleozoic and Mesozoic terranes that originated from the northern margin of Gondwana, splitting from it in the Carboniferous or Permian before subsequently drifting northward to collide with Laurasia in the Mesozoic. However, the paleography and drift history of these terranes remain poorly constrained. Here we present new Middle and Late Permian paleomagnetic data from the North Qiangtang Terrane, which allow us to determine that it drifted from ~24°S to ~9°S from the Middle to Late Permian. On the basis of paleomagnetic and geological data of the Tibetan terranes, we propose that the North Qiangtang Terrane was stably located at ~24°S during the Late Carboniferous and Middle Permian, likely affiliated with the Pamir-Qamdo continental archipelago, and the rapid northward drift of the North Qiangtang terrane starts in the Middle Permian.</p>
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