cometadata/datacite-titles-descriptions-related-identifiers huggingface dataset:
DOI: 10.6084/m9.figshare.21531403.v1
title: Provenance of lower Paleozoic sedimentary rocks in Tasmania and Waratah Bay, southern Victoria: constraints from detrital zircon hafnium isotopes and trace-element geochemistry

description: Nine Paleozoic sedimentary formations from western Tasmania and two from the Lachlan Orogen—one in northeast Tasmania and one in Waratah Bay in Victoria—contain detrital zircons that fall into major U–Pb age clusters at 2.0–1.4, 1.25–0.95 and 0.62–0.49 Ga. The zircon Th/U ratios and rare earth element (REE) patterns suggest a magmatic origin for detrital zircons in all these rock sequences. The REE geochemical signatures on bivariate discrimination diagrams indicate that most of the zircons originated in continental orogenic settings. The oldest group of zircons have a southwest Laurentian signature previously recognised from Proterozoic metasedimentary rocks in Tasmania. The 1.25–0.5 Ga zircons from all the samples have very similar εHf<sub>i</sub> values. They are not statistically different from those of typical Lachlan Orogen sandstones and resemble those in Rodinia and early Gondwana orogenic belts. The εHf<sub>i</sub> values of the Cambrian zircons within the Pioneer Sandstone are similar to the Mount Read Volcanics but cannot be distinguished on εHf<sub>i</sub> values from other sources in East Gondwana. The detrital zircon provenance of the Bear Gully Chert Bed at the base of the Digger Island Marlstone at Waratah Bay includes the west Tasmanian Proterozoic, the East Gondwana margin and the Macquarie Arc. This mixed provenance provides evidence for the late Cambrian docking of VanDieland with East Gondwana. KEY POINTSNew zircon Hf isotope data are reported for early Paleozoic sedimentary rocks in Tasmania and Waratah Bay, southern Victoria.The western Tasmania basement was the dominant source for Tasmanian sandstones and a minor source for the Lachlan Orogen sandstones on the northeast margin of VanDieland.The mixed provenance of the Bear Gully Chert supports a late Cambrian accretion of VanDieland to the East Gondwana margin.The youngest zircons in the Bear Gully Chert at Waratah Bay were potentially sourced from the Macquarie Arc. New zircon Hf isotope data are reported for early Paleozoic sedimentary rocks in Tasmania and Waratah Bay, southern Victoria. The western Tasmania basement was the dominant source for Tasmanian sandstones and a minor source for the Lachlan Orogen sandstones on the northeast margin of VanDieland. The mixed provenance of the Bear Gully Chert supports a late Cambrian accretion of VanDieland to the East Gondwana margin. The youngest zircons in the Bear Gully Chert at Waratah Bay were potentially sourced from the Macquarie Arc.
DOI: 10.6084/m9.figshare.21569043
title: Zircon inheritance, sources of Devonian granitic magmas and crustal structure in central Victoria

description: In central Victoria, inherited zircon in Devonian igneous rocks and detrital zircon in metasedimentary country rocks and an amphibolite-facies xenolith show that Mesoproterozoic parts of the underlying Selwyn Block cannot be the source for all the silicic magmas. Zircon inheritance in S-type samples reveals significant thermal events at 525–425 Ma and 1200–1100 Ma. Both S- and I-type samples have prominent zircon age peaks at 420–410 Ma, which record high-grade metamorphism of the deep crust during the terminal phases of the Benambran and Bindian orogenies. All I-type rocks have 650–500 Ma peaks, suggesting derivation from an arc-related metavolcanic source in the upper Selwyn Block. Protoliths of the greenschist-facies Ordovician metasediments and the amphibolite-facies Cambrian metasedimentary xenolith were deposited in distal backarc settings. Most inherited zircon cores are metamorphic, and the strongest zircon inheritance occurs in hornblende-bearing I-type rocks, highlighting their largely crustal origin. Zircon populations at <i>ca</i> 1400 Ma, thought to signal sediment derivation from East Antarctica and Rodinia-Nuna, are mostly absent in I-type samples and some S-types. The <i>ca</i> 1400 Ma signal probably applies to the upper, metasedimentary Selwyn Block, so Devonian S-type magmas were sourced mainly in the deeper sections. Zircon inheritance in the Devonian igneous rocks was not influenced by the exposed metasedimentary country rocks. Two samples from one of the smaller plutons have contrasting patterns of zircon inheritance, suggesting relatively small-scale source heterogeneity. Many rounded and corroded cores in zircon crystals yield the same ages as the crystallisation dates for the rocks, and thus are antecrysts. Higher whole-rock Zr contents generally correlate with higher proportions of inherited zircon, and differentiation does not affect this relationship. The degree of partial melting of a magma source and the efficiency of crystal entrainment are critical in governing zircon inheritance. Mesoproterozoic sections of the Selwyn Block cannot be the sources for all the Devonian silicic magmas in central Victoria.I-type rocks have 650–500 Ma zircon age peaks, suggesting derivation from arc-related metavolcanic rocks in the upper Selwyn Block.Hornblende-bearing I-type rocks have the strongest zircon inheritance patterns, indicating the largely crustal origins of I-type magmas.Exposed metasedimentary country rocks were not involved in magma genesis. Mesoproterozoic sections of the Selwyn Block cannot be the sources for all the Devonian silicic magmas in central Victoria. I-type rocks have 650–500 Ma zircon age peaks, suggesting derivation from arc-related metavolcanic rocks in the upper Selwyn Block. Hornblende-bearing I-type rocks have the strongest zircon inheritance patterns, indicating the largely crustal origins of I-type magmas. Exposed metasedimentary country rocks were not involved in magma genesis.
DOI: 10.6084/m9.figshare.21569043.v1
title: Zircon inheritance, sources of Devonian granitic magmas and crustal structure in central Victoria

description: In central Victoria, inherited zircon in Devonian igneous rocks and detrital zircon in metasedimentary country rocks and an amphibolite-facies xenolith show that Mesoproterozoic parts of the underlying Selwyn Block cannot be the source for all the silicic magmas. Zircon inheritance in S-type samples reveals significant thermal events at 525–425 Ma and 1200–1100 Ma. Both S- and I-type samples have prominent zircon age peaks at 420–410 Ma, which record high-grade metamorphism of the deep crust during the terminal phases of the Benambran and Bindian orogenies. All I-type rocks have 650–500 Ma peaks, suggesting derivation from an arc-related metavolcanic source in the upper Selwyn Block. Protoliths of the greenschist-facies Ordovician metasediments and the amphibolite-facies Cambrian metasedimentary xenolith were deposited in distal backarc settings. Most inherited zircon cores are metamorphic, and the strongest zircon inheritance occurs in hornblende-bearing I-type rocks, highlighting their largely crustal origin. Zircon populations at <i>ca</i> 1400 Ma, thought to signal sediment derivation from East Antarctica and Rodinia-Nuna, are mostly absent in I-type samples and some S-types. The <i>ca</i> 1400 Ma signal probably applies to the upper, metasedimentary Selwyn Block, so Devonian S-type magmas were sourced mainly in the deeper sections. Zircon inheritance in the Devonian igneous rocks was not influenced by the exposed metasedimentary country rocks. Two samples from one of the smaller plutons have contrasting patterns of zircon inheritance, suggesting relatively small-scale source heterogeneity. Many rounded and corroded cores in zircon crystals yield the same ages as the crystallisation dates for the rocks, and thus are antecrysts. Higher whole-rock Zr contents generally correlate with higher proportions of inherited zircon, and differentiation does not affect this relationship. The degree of partial melting of a magma source and the efficiency of crystal entrainment are critical in governing zircon inheritance. Mesoproterozoic sections of the Selwyn Block cannot be the sources for all the Devonian silicic magmas in central Victoria.I-type rocks have 650–500 Ma zircon age peaks, suggesting derivation from arc-related metavolcanic rocks in the upper Selwyn Block.Hornblende-bearing I-type rocks have the strongest zircon inheritance patterns, indicating the largely crustal origins of I-type magmas.Exposed metasedimentary country rocks were not involved in magma genesis. Mesoproterozoic sections of the Selwyn Block cannot be the sources for all the Devonian silicic magmas in central Victoria. I-type rocks have 650–500 Ma zircon age peaks, suggesting derivation from arc-related metavolcanic rocks in the upper Selwyn Block. Hornblende-bearing I-type rocks have the strongest zircon inheritance patterns, indicating the largely crustal origins of I-type magmas. Exposed metasedimentary country rocks were not involved in magma genesis.
DOI: 10.6084/m9.figshare.21405567.v1
title: Evolution of diagenetic fluids in the deeply buried, upper Ediacaran Dengying Formation, Central Sichuan Basin, China

description: Deeply buried Precambrian carbonate reservoirs host economic petroleum reserves. The upper Ediacaran Dengying Formation (maximum burial depth &gt;8 km) is predominantly composed of dolostone with porosity ranging from 2 to 4%, and minor limestone with a porosity of &lt;2%. Detailed petrological observations and high-resolution geochemical analyses show the evolution from depositional fluids to late diagenetic fluids. Dolostone is subdivided into dolo-mudstone, dolo-laminite, stromatolitic dolostone, thrombolitic dolostone and oncoidal dolostone. These dolostones were precipitated from the Ediacaran seawater and yield rare earth elements and yttrium (REY) patterns similar to those of modern seawater. In the early diagenetic regimes, fibrous dolomite cement, characterised by superchondritic Y/Ho ratios, was first precipitated from marine porewaters, and then fine-crystalline dolomite cement, characterised by low Y/Ho ratios, was formed during meteoric diagenesis. Bladed dolomite cement was subsequently precipitated from (modified) seawater-dominated porewaters. In the intermediate burial regimes, medium- to coarse-crystalline dolomite cement was formed during reduction of Mn oxides. In the deep-burial regimes, saddle dolomite was precipitated from hydrothermal fluids and yields REY patterns characterised by MREE enrichment. Its superchondritic Y/Ho ratios were likely caused by the fractionation between Y and Ho during the co-precipitation of fluorite. Calcite cement has similar parent fluids to those of saddle dolomite. These dolomite phases have similar δ<sup>13</sup>C values, while their δ<sup>18</sup>O values gradually decrease during the paragenetic sequence. Multiphase dolomitisation led to the increase in Ca/Mg ratios of formation water and reservoir performance. This study is significant for those concerned with the deeply buried dolostone reservoirs. KEY POINTSMicrobialites and five types of dolomite cements have different REY patterns.Co-precipitation of fluorite led to the superchondritic Y/Ho ratios of dolomite.Dolomite and calcite grains show micro-scale geochemical variations.This dolostone reservoir underwent multiphase fluids, including meteoric water, seawater and hydrothermal fluid. Microbialites and five types of dolomite cements have different REY patterns. Co-precipitation of fluorite led to the superchondritic Y/Ho ratios of dolomite. Dolomite and calcite grains show micro-scale geochemical variations. This dolostone reservoir underwent multiphase fluids, including meteoric water, seawater and hydrothermal fluid.
DOI: 10.6084/m9.figshare.21548389.v1
title: Aluminium-normalised trace-element paleoredox proxies and their application to the study of the conditions of Burgess Shale-type preservation

description: The paleo-ecological settings of Burgess Shale-type (BST) fossils have been the subject of extensive investigations, particularly with regard to the role of anoxia in their exceptional preservation. Our understanding of the complexity of both paleontological and geochemical environmental proxies has evolved with increased knowledge of niche communities and marine geochemical and biogeochemical processes. Accordingly, dated approaches should be reevaluated. The commonly applied paleoredox proxies V/Cr, Ni/Co, and V/(V + Ni), as well as the redox proxy V/Al<sub>2</sub>O<sub>3</sub> and productivity proxy Ba/Al<sub>2</sub>O<sub>3</sub>, were all tested on the Wheeler Formation (Utah, USA) for which a fluctuating oxycline environment has been well established based on paleontological features. Subsequently, these proxies were applied to three additional BST fossil-bearing deposits: the Emigsville Member of the Kinzers Formation (Pennsylvania, USA), the Burgess Shale (British Columbia, CA) and the Emu Bay Shale (South Australia, AU). Their host shales lack perceptible V of marine origin, indicative of oxic conditions, in contrast to the Wheeler and brine-related strata from the Burgess Shale which include additional marine input of V in some beds, consistent with varying redox conditions. The black shales of the Longs Park Member (Kinzers) have elevated V/Al<sub>2</sub>O<sub>3</sub> indicative of anoxic conditions. Molybdenum concentrations are relatively low in most samples, but minor variations tend to correlate with V/Al<sub>2</sub>O<sub>3</sub> patterns. Ba/Al<sub>2</sub>O<sub>3</sub> indicates high productivity with deposition of BST fossils in the Wheeler Formation, and diagenetic remobilisation of Ba owing to sediment anoxia in the Burgess Shale. Our findings show that redox proxy V/Al<sub>2</sub>O<sub>3</sub> can be effectively applied to BST samples, whereas Ba/Al is a reliable proxy for low to moderate paleoproductivity levels and may be useful as a secondary or tangential proxy for redox conditions. Taphonomic processes leading to BST preservation occur in a variety of environments characterised by oxyclines, matgrounds, variable sedimentation rates, hypersalinity and/or anoxia.KEY POINTSV/Al<sub>2</sub>O<sub>3</sub> and Ba/Al<sub>2</sub>O<sub>3</sub> are effective proxies for anoxia and productivity in BST deposits.BST preservation can occur in a variety of depositional environments.Marine anoxia is not required for BST preservation. V/Al<sub>2</sub>O<sub>3</sub> and Ba/Al<sub>2</sub>O<sub>3</sub> are effective proxies for anoxia and productivity in BST deposits. BST preservation can occur in a variety of depositional environments. Marine anoxia is not required for BST preservation.
DOI: 10.6084/m9.figshare.21548389
title: Aluminium-normalised trace-element paleoredox proxies and their application to the study of the conditions of Burgess Shale-type preservation

description: The paleo-ecological settings of Burgess Shale-type (BST) fossils have been the subject of extensive investigations, particularly with regard to the role of anoxia in their exceptional preservation. Our understanding of the complexity of both paleontological and geochemical environmental proxies has evolved with increased knowledge of niche communities and marine geochemical and biogeochemical processes. Accordingly, dated approaches should be reevaluated. The commonly applied paleoredox proxies V/Cr, Ni/Co, and V/(V + Ni), as well as the redox proxy V/Al<sub>2</sub>O<sub>3</sub> and productivity proxy Ba/Al<sub>2</sub>O<sub>3</sub>, were all tested on the Wheeler Formation (Utah, USA) for which a fluctuating oxycline environment has been well established based on paleontological features. Subsequently, these proxies were applied to three additional BST fossil-bearing deposits: the Emigsville Member of the Kinzers Formation (Pennsylvania, USA), the Burgess Shale (British Columbia, CA) and the Emu Bay Shale (South Australia, AU). Their host shales lack perceptible V of marine origin, indicative of oxic conditions, in contrast to the Wheeler and brine-related strata from the Burgess Shale which include additional marine input of V in some beds, consistent with varying redox conditions. The black shales of the Longs Park Member (Kinzers) have elevated V/Al<sub>2</sub>O<sub>3</sub> indicative of anoxic conditions. Molybdenum concentrations are relatively low in most samples, but minor variations tend to correlate with V/Al<sub>2</sub>O<sub>3</sub> patterns. Ba/Al<sub>2</sub>O<sub>3</sub> indicates high productivity with deposition of BST fossils in the Wheeler Formation, and diagenetic remobilisation of Ba owing to sediment anoxia in the Burgess Shale. Our findings show that redox proxy V/Al<sub>2</sub>O<sub>3</sub> can be effectively applied to BST samples, whereas Ba/Al is a reliable proxy for low to moderate paleoproductivity levels and may be useful as a secondary or tangential proxy for redox conditions. Taphonomic processes leading to BST preservation occur in a variety of environments characterised by oxyclines, matgrounds, variable sedimentation rates, hypersalinity and/or anoxia.KEY POINTSV/Al<sub>2</sub>O<sub>3</sub> and Ba/Al<sub>2</sub>O<sub>3</sub> are effective proxies for anoxia and productivity in BST deposits.BST preservation can occur in a variety of depositional environments.Marine anoxia is not required for BST preservation. V/Al<sub>2</sub>O<sub>3</sub> and Ba/Al<sub>2</sub>O<sub>3</sub> are effective proxies for anoxia and productivity in BST deposits. BST preservation can occur in a variety of depositional environments. Marine anoxia is not required for BST preservation.
DOI: 10.34740/kaggle/dsv/5071384
title: 🇺🇦 Ukraine Conflict Twitter Dataset
DOI: 10.5281/zenodo.7679403
title: MAGICC7 SSP carbon cycle output using AR6 tuning

description: Output from the MAGICC7 carbon cycle model under the SSP scenarios with the configuration used in IPCC AR6. For further details on MAGICC and expectations re use of data and the model, please see https://magicc.org/download/magicc7.
DOI: 10.5281/zenodo.7679402
title: MAGICC7 SSP carbon cycle output using AR6 tuning

description: Output from the MAGICC7 carbon cycle model under the SSP scenarios with the configuration used in IPCC AR6. For further details on MAGICC and expectations re use of data and the model, please see https://magicc.org/download/magicc7.
DOI: 10.6084/m9.figshare.22180351
title: transboundary transport of soot particles

description: ageing processes of soot particles during transboundary transport
DOI: 10.6084/m9.figshare.22180354
title: Stranded Traveller Survey Data

description: This study aimed to evaluate the psychological and financial distress reported by citizens and permanent residents stranded abroad due to international travel restrictions introduced in response to the COVID-19 pandemic.
DOI: 10.5439/1258772
title: aoshumidigraph.a1

description: various temperatures, pressures, RH, flows for the AOS humidograph system. This system controls the humidity of the air that is supplied to the dry and wet nephelometers.
DOI: 10.25582/data.2022-03.2444386/1910309
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444476/1910322
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444422/1910349
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444211/1910363
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444201/1910371
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444212/1910379
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444370/1910387
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444471/1910395
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444385/1910409
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444382/1910437
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444384/1910449
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444461/1910459
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444213/1910471
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444210/1910476
title: Data for EMSL Project 51134 from March 2022
DOI: 10.25582/data.2022-03.2444653/1933973
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444807/1934016
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444822/1934039
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444747/1934055
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444776/1934139
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444758/1934148
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444770/1934183
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444789/1934304
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444803/1934307
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444751/1934338
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444774/1935254
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444813/1935255
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444752/1935285
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444650/1935290
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444867/1935341
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444763/1935359
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444762/1935444
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444885/1936204
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444750/1936241
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444800/1936310
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444756/1936338
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444767/1936424
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444884/1937264
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444799/1937341
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444775/1937361
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444749/1937401
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444793/1937463
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444748/1937516
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444772/1937560
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444833/1937590
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444764/1937603
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444790/1937956
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444817/1937980
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444757/1938050
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444765/1938084
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444645/1938170
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444829/1938184
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444812/1939060
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444761/1939184
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444766/1939218
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444639/1939257
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444792/1939300
title: Data for EMSL Project 51132 from March 2022
DOI: 10.25582/data.2022-03.2444880/1939355
title: Data for EMSL Project 51132 from March 2022