cometadata/datacite-titles-descriptions-related-identifiers huggingface dataset:
DOI: 10.35003/j0culj
title: Replication Data for: Studying the Global Spatial Randomness of Impact Craters on Mercury, Venus, and the Moon With Geodesic Neighborhood Relationship

description: • We improve approaches to quantify the spatial randomness of impact craters by applying geodesic methods • We apply these methods to analyze the global spatial randomness of impact crater populations on Mercury, Venus, and the Moon • We use the results to investigate known crater population variations and surface evolution scenarios on Mercury, Venus, and the Moon This is Version 2, Version 1 is stored in Mendeley, http://dx.doi.org/10.17632/mn2b542k5r.2
DOI: 10.35003/j0culj/csukda
title: Description-1.txt

description: :unav
DOI: 10.35003/j0culj/ayevmj
title: 01_Script.exe

description: Python 2.* script to conduct global randomness analyses of impact craters - Description of the variables to be changed in the Python script
DOI: 10.35003/j0culj/q8noqh
title: 02_Results.exe

description: Contains the results of the randomness analysis of global crater data sets (Mercury, Venus, and the Moon) in the form of histogram and map plots, as well as Z-score plots
DOI: 10.35003/j0culj/zigjse
title: 2020je006693-sup-0001-supporting information si-s01.docx

description: Supporting Information 1
DOI: 10.35003/ebulmm/dpztxy
title: fig2.tab

description: :unav
DOI: 10.35003/ebulmm/zqa7an
title: fig1b_vertical_evolving.tab

description: :unav
DOI: 10.35003/ebulmm/py3lmj
title: fig1c_size_scale.tab

description: :unav
DOI: 10.35003/ebulmm/usqmii
title: fig1e_map_3.8Ga.tab

description: :unav
DOI: 10.35003/ebulmm/cxbi31
title: fig1f_map_highly_fractured_depth.tab

description: :unav
DOI: 10.35003/ebulmm
title: Replication Data for: 3D-simulation of Lunar Megaregolith Evolution: Quantitative Constraints on Spatial Variation and Size of Fragment

description: • A 3D numerical model was built to quantitatively constrain the distribution of lunar megaregolith and its fragment size. • Megaregolith has a distinct spatial variation and the size of fragments in the top 2 km is generally four orders of magnitude smaller than that deeper than 10 km. • Basin-forming events controlled the megaregolith growth where the SPA impact shaped its structure.
DOI: 10.35003/ebulmm/2ee3ov
title: fig1a_crater_distribution.tab

description: :unav
DOI: 10.35003/ebulmm/n9tyxx
title: fig1d_map_4.3Ga.tab

description: :unav
DOI: 10.5281/zenodo.7655081
title: Lateral flow immunoassay-based laboratory algorithm for rapid diagnosis of diphtheria

description: <strong>List of corynebacteria strains used in the Diphtheria Lateral Flow Immunoassay (LFIA) development and evaluation study and their <em>tox</em> (by PCR) and Tox (by Elek test and LFIA) status</strong>
DOI: 10.5281/zenodo.7655080
title: Lateral flow immunoassay-based laboratory algorithm for rapid diagnosis of diphtheria

description: <strong>Results of the ‘DIFTERIA’ Lateral Flow Immunoassay (LFIA) validation</strong>
DOI: 10.5281/zenodo.7689813
title: Lateral flow immunoassay-based laboratory algorithm for rapid diagnosis of diphtheria

description: <strong>Results of the ‘DIFTERIA’ Lateral Flow Immunoassay (LFIA) validation. </strong>
DOI: 10.5281/zenodo.7689924
title: Lateral flow immunoassay-based laboratory algorithm for rapid diagnosis of diphtheria

description: <strong>Results of the ‘DIFTERIA’ Lateral Flow Immunoassay (LFIA) validation. </strong>
DOI: 10.5281/zenodo.7706857
title: Lateral flow immunoassay-based laboratory algorithm for rapid diagnosis of diphtheria

description: <strong>Results of the ‘DIFTERIA’ Lateral Flow Immunoassay (LFIA) validation. </strong>
DOI: 10.5281/zenodo.7827917
title: Lateral flow immunoassay-based laboratory algorithm for rapid diagnosis of diphtheria

description: <strong>Results of the ‘DIFTERIA’ Lateral Flow Immunoassay (LFIA) validation</strong>
DOI: 10.35003/xkkp5t/xyyxjq
title: Supp_Material_2.pdf

description: Profiles of the experimental runs
DOI: 10.35003/xkkp5t/2nwi3t
title: Supp_Material_1.tab

description: Tables: Major element composition and halogen content , recalculation of an EDS/WDS amphibole, F, Cl and Br contents of reference glasses and minerals
DOI: 10.35003/xkkp5t/tswvbq
title: 1-s2.0-S0024493720304941-gr7_lrg.jpg

description: Fig. 7. F/Nd vs F content of partial melts: Calculated F/Nd of melts derived from metasomatized mantle sources with different modal abundances of amphibole and mica (blue lines). The black dashed line, depicted as DM, shows the evolution of melts derived from a depleted MORB mantle with F and Nd contents after Salters and Stracke (2004). The black dashed line, depicted as EM, represents F/Nd of melts coming from a relatively enriched MORB mantle source (Donnelly et al., 2004; Shimizu et al., 2016) The light grey area depicts calculated F/Nd of melts that were derived from an amphibole and/or mica bearing source. The green line shows the F/Nd values of melts coming from a F-rich source (1amp-4mica). The dark grey area shows the overlap of the F/Nd values between metasomatized and F-rich sources (different F, Nd contents, minerals abundances and degrees of partial melting). The black dashed curves represent the best fit of similar degrees of melting for the metasomatized sources, calculated from our model. After 10% of melting the melts from the source “10.5 amp – 2.9 mica” will have a F/Nd of ~130, while the melts from the source “4 amp – 1 mica” will have F/Nd of ~95. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/xkkp5t/vvd9dx
title: 1-s2.0-S0024493720304941-gr4_lrg.jpg

description: Fig. 4. F/Cl vs F content of partial melts: Calculated F/Cl of melts derived from metasomatized mantle sources with different modal abundances of amphibole and mica (blue lines). The black dashed lines denoted as DM and EM, show the F/Cl ratio of melts from an anhydrous mantle (without amphibole and mica) with a DM halogen content after Salters and Stracke (2004), and relatively elevated halogen content (EM) after Shimizu et al. (2016) The grey area depicts our modeled metasomatized mantle based on the calculated F/Cl of melts that were derived from amphibole and/or mica bearing sources with DF &gt; 1 (for both of these phases). The blue dotted curves represent the best fit of similar degrees of melting for the metasomatized sources, calculated from our model. For example, after 5% of melting the melts from the source “10.5 amph – 2.9 mica” will have a F/Cl of ~7, while the melts from the source “4 amph – 1 mica” will have F/Cl of ~15. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/xkkp5t/9ocquw
title: 1-s2.0-S0024493720304941-gr1_lrg.jpg

description: Fig. 1. Representative backscattered electron (BSE) images of experimental run products. A: run SFE1-BSN2. Mineral phases present are amph, cpx, opx and glass; B: run SFE1-BSN1. Mineral phases present are amph, ol and glass; C: run SFE2-BSN2. Mineral phases present are amph, phl, cpx, opx and glass; D: run SFE2-BSN1. Mineral phases present are amph, cpx, ol and glass.
DOI: 10.35003/xkkp5t/evhg0e
title: 1-s2.0-S0024493720304941-gr5_lrg.jpg

description: Fig. 5. F/Cl vs F content of partial melts, for metasomatized sources (MM) with amphibole and mica when DF &gt; 1 for both phases (left side of the Figure), and for DF &lt; 1 for both phases (right side of the Figure). Blue lines show the F/Cl of melts derived from MM sources with DF &gt; 1, while the red lines represent the exact same sources but for a DF &lt; 1. Grey areas depict our modeled MM for each individual case of DF values. Degrees of melting are shown for each set of sources in blue and orange dashed lines. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/xkkp5t/f9aieu
title: 1-s2.0-S0024493720304941-gr8_lrg.jpg

description: Fig. 8. F/Cl and F/Nd vs F content of partial melts: Calculated ratios of melts derived from metasomatized mantle sources with different modal abundances of amphibole and mica (colored lines), e.g. the blue line represents F/Nd of melts derived from peridotite that contains 4% of amphibole and 1% of phlogopite. The black dashed lines show the F/Cl and F/Nd of an unmetasomatized (without amphibole or mica) depleted mantle. The plotted F/Cl, F/Nd data come from olivine-hosted melt inclusions from a variety of tectonic settings reported in different studies, 1 Saal et al., 2002; 2 Shimizu et al., 2019; 3 Cabral et al., 2014; 4 Métrich et al., 2014; 5 Rose-Koga et al., 2012; 6 Portnyagin et al., 2007; 7 Vigoroux et al., 2008; 8 Gazel et al., 2012. F/Nd ratios of olivine hosted melt inclusions from basalts have been used to identify source compositions of a depleted mantle (Workman et al., 2006), while F/Cl have not been used before. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/xkkp5t/9s4mrk
title: 1-s2.0-S0024493720304941-gr3_lrg.jpg

description: Fig. 3. DF (cpx/melt) plotted against major element composition of run products clinopyroxenes; left: DF (cpx/melt) plotted against Al in octahedral coordination; right: F partition coefficients (DF cpx/melt) plotted against Ti in hexagonal coordination. Errors reported are 3-S.D.
DOI: 10.35003/xkkp5t/fgmwsa
title: 1-s2.0-S0024493720304941-gr6_lrg.jpg

description: Fig. 6. F/Cl vs F content of partial melts for metasomatized mantle sources (blue lines) and F-rich sources (green lines), for different modal abundances of amphibole and mica. The grey area represents the possible F/Cl values of melts derived from metasomatized mantle sources, while the light green area represents possible values of melts derived from F-rich sources. The dark green area represents the overlap of F/Cl values between sources that have different halogen contents, mineral abundances and underwent different degrees of partial melting. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/xkkp5t/plyfub
title: Table_3.tab

description: Table 3. Our new mineral/melt partition coefficients of F and Cl.
DOI: 10.35003/xkkp5t/vpjqv1
title: 1-s2.0-S0024493720304941-gr2_lrg.jpg

description: Fig. 2. DF (amph or phl/melt) plotted against major element composition of amphiboles or mica. Depicted are top left: DF (amph/melt) partition coefficients plotted against Ti in amphibole in octahedral coordination; top right: DF (amph/melt) plotted against DF (phl/melt) in the experiments that both phases are present. Mica; bottom left; right: DF (mica/melt) plotted against K and Na in the octahedral sites of mica. Errors are 2-S.D.
DOI: 10.35003/xkkp5t/xfknwd
title: Table_2.tab

description: Table 2. Experimental conditions and results.
DOI: 10.35003/xkkp5t/8qpqxk
title: Table_1.tab

description: Table 1. Starting material compositions.
DOI: 10.35003/xkkp5t/gg8iu2
title: Table_4.tab

description: Table 4. Modal amounts and halogen contents (ppm) of minerals of the modeled sources.
DOI: 10.35003/xkkp5t/oqxw0o
title: Table_5.tab

description: Table 5. Partition coefficients used in the melting model.
DOI: 10.35003/iluu2b
title: Replication Data for: An Improved Electron Microprobe Method for the Analysis of Halogens in Natural Silicate Glasses

description: We present a new analytical method, which allows the simultaneous analysis of fluorine (F), chlorine (Cl), bromine (Br), and iodine (I) in geological samples. To account for interferences of Fe on the spectral lines of F, of Al on Br-lines, and of Ca on I-lines, we prepared four new halogen-free calibration glasses. The new method is used to analyze various glass reference materials and crystal-hosted melt inclusions from the Azores. Our results show that our new method allows reliable and reproducible analyses of all four halogens in silicate glasses.
DOI: 10.35003/iluu2b/3wdfl6
title: S1431927620013495sup001.tab

description: supplementary material 1
DOI: 10.35003/iluu2b/aszpa0
title: An-improved-electron-microprobe-method-for-the-analysis-of-halogens-in-natural-silicate-glasses.pdf

description: open access manuscript
DOI: 10.35003/iluu2b/p9mhvj
title: S1431927620013495sup002.tab

description: supplementary material 2
DOI: 10.35003/iluu2b/vq2lix
title: tab3.png

description: Table 3. Fluorine and Cl Contents of Reference Glasses from the Literature Compared With Our Study.
DOI: 10.35003/iluu2b/a6n3v5
title: tab2.png

description: Table 2. Reference Glasses Analyzed in the Present Study and Their F, Cl contents (μg/g).
DOI: 10.35003/iluu2b/gzgfse
title: tab4.png

description: Table 4. Bromine Contents (μg/g) and Accuracy of Reference Glasses Analyzed in Our Study and in Cadoux et al. (2017).
DOI: 10.35003/iluu2b/xtv7nv
title: tab5.png

description: Table 5. Major Elements (wt%) and Halogen Concentrations (μg/g) of Experimental Glasses.
DOI: 10.35003/iluu2b/p43tlf
title: tab1.png

description: Table 1. Major Elements (wt%) Composition and “Apparent” Halogen Contents (μg/g) of Halogen-Free Glasses Used for the Calibration.
DOI: 10.35003/iluu2b/4f5awn
title: fig3.png

description: Fig. 3. Fluorine versus Cl data in olivine-hosted melt inclusions from the Azores show good agreement between datasets obtained with different instruments and methods. Particularly, the two datasets obtained on melt inclusions from Pico island span the same Cl–F space. 1Present study, 2Métrich et al. (2014), and 3Rose-Koga et al. (2017). The table with the individual data can be found in Supplementary Table 2.
DOI: 10.35003/iluu2b/lkgvcw
title: fig2.png

description: Fig. 2. (a) Fluorine literature data for the glasses VG-A99, VGA-568, VG-2, AC-E, DR-N, GS-N, BCR-2G, and BHVO2-G (Marks et al., 2016; Zhang et al., 2016), compared with F data from the present study. Fluorine concentrations from each study can be found in Tables 2 and 3. The dashed line represents the 1:1 line. Our results are plotted mainly against the data from Zhang et al. (2016), in order to show the good agreement of the individual studies. Glasses VGA-568, VG-A99, and VG-2 show differences that are discussed inside the text and are attributed to glass inhomogeneity. (b) Chlorine literature data for the glasses VG-A99, VGA-568, VG-2, AC-E, DR-N, GS-N, BCR-2G, and BHVO2-G (Marks et al., 2016; Zhang et al., 2016), compared with Cl data from the present study. Chlorine concentrations from each study can be found in Tables 2 and 3. The dashed line represents the 1:1 line. Our results are plotted mainly against the data from Zhang et al. (2016) and show an overall excellent agreement.
DOI: 10.35003/iluu2b/yao2kj
title: fig1.png

description: Fig. 1. (a) Calibration line for F. Glasses with different Fe contents were used from ~0.4 to ~14 wt% (Table 1). There is an almost linear correlation (R2 = 0.9962) with increasing Fe content. The 95.45% confidence line indicates that the error (2 SD) on the F content because of Fe is relatively small (±40 μg/g) up to ~9 wt% and increases (±80 μg/g) at higher concentrations. (b) Calibration line for Br that quantifies the effect of Al in the analysis signal. Our glasses have an Al2O3 content ranging from ~1 to ~18 wt% (Table 1). The excess Br signal we get from Al also shows a linear relation (R2 = 0.9891) with an increasing amount of Al inside the samples. Based on the 95.45% confidence lines, the error (2 SD) at the excess Br for Al concentrations higher than 12 wt% is ±20 μg/g, while it increases significantly at concentrations less than 2 wt%, probably due to the absence of glasses with very low Al contents. (c) Calibration line for I shows the effect of Ca-interference on the I measurements. The Ca compositional range of our glasses is from 0.4 to ~14 wt% (Table 1). The correlation between the glasses with different Ca contents and the excess I in the signal of the analysis has a linear correlation (R2 = 0.9958). The 95% confidence lines show that the error (2 SD) at the excess I for Ca concentrations from ~5 to ~14 wt% is ±20 μg/g, while it increases at low concentrations (&lt;2 wt%) at 40 μg/g.
DOI: 10.35003/bmfshw
title: Replication Data for: Chalcophile elements in Martian meteorites indicate low sulfur content in the Martian interior and a volatile element-depleted late veneer.

description: • Ratios of Cu, S, Se, Te, Re, Pt and Pd in Martian meteorites are relatively constant. • Martian meteorites show very limited eruptive losses of volatile Re, S, Se and Te. • The parent magmas of most Martian meteorites were sulfide-undersaturated. • Martian mantle and core have a low sulfur content. • Low Te/PGE ratios in Martian meteorites reflect a strongly volatile element-depleted Martian late veneer.
DOI: 10.35003/bmfshw/qfdjzy
title: 1-s2.0-S0012821X17300353-mmc1.docx

description: MMC 1. The supplementary materials include the details of analytical methods, two supplementary figures and references for initial ε143Nd used in Table 1.
DOI: 10.35003/bmfshw/ps2iuz
title: 1-s2.0-S0012821X17300353-mmc2.tab

description: Table S1. Summary of Martian meteorites analyzed in this study.
DOI: 10.35003/bmfshw/yceg2o
title: 1-s2.0-S0012821X17300353-mmc3.tab

description: Supplementary Table 2. Results of Cu, S, Se and Te contents of Martian meteorites by isotope dilution ICP-MS and comparison with literature data (red color).
DOI: 10.35003/bmfshw/vsvoq1
title: 1-s2.0-S0012821X17300353-gr008.sml

description: Fig. 8. Schematic depiction of the final stages of core formation on Mars and Earth and subsequent late accretion. Sulfur, Se and Te in the mantle of Earth and Mars in combination with approximately chondritic HSE ratios require late accretion of volatile element-depleted and -undepleted material onto Mars (this work) and Earth (Wang and Becker, 2013), respectively. The final stages of Martian core formation occurred much earlier (e.g., Dauphas and Pourmand, 2011) than on Earth (Jacobson et al., 2014). The ‘dry’ Martian late veneer implies that the Martian water was delivered before the late veneer. See text for details.
DOI: 10.35003/bmfshw/1fg6ld
title: 1-s2.0-S0012821X17300353-gr003.sml

description: Fig. 3. Variation of ratios of Cu, S, Se and Te in Martian meteorites with MgO contents. These element ratios display limited variations for most samples, including different groups of shergottites and nakhlites (except Nakhla). The behavior of the shergottite data differ from the evolution trend of sulfide saturated terrestrial MORB (Jenner and O'Neill, 2012, Lissner et al., 2014) and terrestrial cumulate rocks (Wang and Becker, 2015a), which show strong fractionation of Cu, Se and Te because of different sulfide–silicate melt partition coefficients (Te &gt; Cu &gt; Se ≥ S). S/Se ratios change little during melting and fractional crystallization of basalts, even if sulfide saturation was attained (Jenner and O'Neill, 2012, Wang and Becker, 2015a). Occasionally high S/Se ratios in Martian meteorites (e.g., RBT04262, MIL03346 and LAR06319) reflect assimilation of S from the Martian crust. Blue bands are the ranges of ratios (±1s) in most of the analyzed meteorites (Table 1). Differences between data from the present study and literature data for individual meteorites (Meyer, 2013, Smith et al., 1984, Treiman et al., 1986, Wang et al., 1998; Table S2) are indicated by the dashed line. Error bars (1s) are shown for the new data and most errors are smaller than symbol sizes. (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/bmfshw/35get9
title: 1-s2.0-S0012821X17300353-gr007.sml

description: Fig. 7. CI chondrite normalized abundances of S, Se, Te, Cu and highly siderophile elements in the mantles of Mars and Earth (this study; Becker et al., 2006, Lodders, 2003, Taylor, 2013, Wang and Becker, 2013). The Martian mantle is strongly depleted in Te, which yields a maximum value for the contribution of Te from metal–silicate partitioning during core formation. This value also indicates late accretion of a strongly volatile element-depleted late veneer on Mars. In contrast, Cu, S and Se in the Martian mantle are primarily left over from metal–silicate segregation. Among chondrites, H chondrites (a) have the lowest Te/Ir and Te/Se ratios (Wasson and Kallemeyn, 1988). The pattern b) represents an alternative composition of volatile element-depleted late accreted material with ratios of volatile elements similar to CI chondrites. (For interpretation of the references to color in this figure, the reader is referred to the web version of this article.)
DOI: 10.35003/bmfshw/wuecmi
title: 1-s2.0-S0012821X17300353-gr005.sml

description: Fig. 5. Ratios of Cu/Se versus CI chondrite normalized La/Yb(N) and ε143Ndinitial, respectively. a) Shergottites and some nakhlites (except Nakhla) have similar Cu/Se ratios. Data source from Table 1. b) Shergottites from different mantle sources show relatively constant Cu/Se ratios. ε143Ndinitial data sources are given in Table 1. The original references are listed in the supplement.
DOI: 10.35003/bmfshw/aezzma
title: 1-s2.0-S0012821X17300353-gr004.sml

description: Fig. 4. Cu/Pd ratios in shergottites and in terrestrial mantle-derived magmatic rocks. Because sulfide–silicate melt partition coefficients of Cu (∼103) and Pd (∼105–106) are very different (Mungall and Brenan, 2014), sulfide saturation and segregation during fractional crystallization leads to highly variable Cu/Pd in evolving melts and cumulates, e.g., up to 3 orders of magnitude in lower crustal gabbros (Peucker-Ehrenbrink et al., 2012) and in MORB glasses (e.g., Lissner et al., 2014). In contrast, terrestrial komatiites from Victoria's lava lake (Puchtel et al., 2016) display constant Cu/Pd in rocks that display a range of MgO contents. Note Cu/Pd ratios of these komatiites overlap Cu/Pd of Earth's mantle, indicating that the Cu/Pd ratio of sulfide-undersaturated magma generally reflects its mantle source. As in terrestrial komatiites, Cu/Pd in most shergottites are relatively constant (2650 ± 950, blue band) over a large range of MgO contents, consistent with sulfide-undersaturated magmatic evolution. The mean Cu/Pd of shergottites is slightly higher than that calculated from Cu and Pd contents of the Martian mantle because of the large uncertainty of the estimated Pd value of the Martian mantle (Day et al., 2016, Taylor, 2013). Literature Pd contents in shergottites are from Brandon et al. (2012), and the corresponding Cu contents are from this study and Meyer (2013). Because of sample heterogeneity, literature data on Y-980459 and Dhofar 019 display highly variable PGE contents and thus Cu data obtained on different aliquots yield apparently different Cu/Pd (gray symbols with dashed lines). The Pd value of a replicate of Dhofar 019 is from Jones et al. (2003) whereas a lower Pd content for Y-980459 was measured by Yang et al. (2015). Because Cu and Pd contents are not from the same sample aliquots, this contributes to the scatter of Cu/Pd ratios (a factor of 3–4 variation). (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.)
DOI: 10.35003/bmfshw/9mkg8m
title: 1-s2.0-S0012821X17300353-gr006.sml

description: Fig. 6. Fractionation of ratios of Pt and Pd with Ir in different groups of shergottites. The strong fractionation of Pd/Ir and Pt/Ir by three orders of magnitude, but limited fractionation of Pt/Pd indicates sulfide-undersaturated magmatic evolution (a). Lherzolitic shergottites have Pt/Pd similar to CI chondrites, whereas olivine-phyric and basaltic shergottites display a mean Pt/Pd of 0.84, which is slightly lower than the value of CI chondrites (a). Pd/Pt ratios show limited variations of less than a factor of 3 in depleted, intermediate and enriched shergottites (b). Data from Brandon et al. (2012).