cometadata/datacite-titles-descriptions-related-identifiers huggingface dataset:
DOI: 10.1594/pangaea.933563
title: GEM-2 combined snow and ice thickness within the laser scanning area on station PS81/506_GPS1

description: Combined snow and ice thickness from a multifrequency electromagnetic induction instrument (GEM-2) in the terrestrial laser scanning (TLS) area, see Hunkeler et al. (2015) for details. GEM-2 was performed inside the laser scan field after all scans had been acquired.
description: Coordinates:============X and Y coordinates are relative to a GPS base station installed on each floe. Coordinates were determined using post-processing kinematic GPS (PPK-GPS), and corrected for floe ration and drift. Coordinates of measurements inside the laser scanning area were particularly carefully processed to collocate measurements as accurately as possible (within a few cm). The vertical height above sea level in the TLS data was determined by using reflectors on poles. Upon installation of these reflector poles, the ice was drilled through and the height of the reflector above sea level was determined. For details, see Wever et al. (2021).On the floe scale walk, magnaprobe coordinates have been equally processed as in the laser scanning area. However, for the GEM-2 instrument, the position of the magnaprobe was taken for the corresponding time stamp in the GEM-2 data. Since the GEM-2 instrument was following the Magnaprobe surveyor with a few m distance, this leads to less precise positioning. However, the GEM-2 instrument also has a footprint of similar order of magnitude (see Hunkeler et al., 2015).Coordinate reference points:============================All coordinates are relative to GPS base station 1, in a local coordinate system where X and Y coordinates align with easting and northing, respectively, from the respective UTM Zone at a specific point in time. The respective coordinates of GPS base station 1 for this dataset are:For PS81/506: Location of GPS base station 1, July 12 2013, 2000 UTC:WGS84 : latitude=-67.19689 longitude=-23.15692UTM Zone 27S : northing=2545052 easting=406729
DOI: 10.1594/pangaea.967641
title: d13C values measured by Secondary Ion Mass Spectrometry in shells of the planktic foraminifer Morozovella allisonensis from the PETM section of ODP Site 865 (Central Pacific)

description: Foraminiferal shells of the species M. allisonensis from the PETM section of ODP Site 865, Central Pacific, were cast with 3 grains of UWC-3 calcite standard (Kozdon et al., 2009) in the center of a 25 mm round epoxy mount, ground to the level of best exposure, polished, cleaned, and Au-coated. Prior to geochemical analysis, shells were examined by Scanning Electron Microscopy (SEM) to identify subdomains suitable for in-situ d13C and Mg/Ca ratio measurements and to avoid diagenetically altered zones within each shell. In-situ d13C measurements were performed with ~7 µm beam spot size in the WiscSIMS Laboratory at UW-Madison by a CAMECA ims-1280 large radius multicollector ion microprobe) using the protocols described in a previous study (Kozdon et al., 2018). The in-situ d13C microanalyses primarily targeted subdomains located at the base of pustular outgrowths (muricae) along the chamber walls of each shell. Previous studies have shown that these subdomains are less susceptible to post-depositional alteration than the rest of the shell (Kozdon et al., 2011; Kozdon et al., 2013). Between one and five SIMS d13C microanalyses were performed for each shell. Reproducibility of the individual spot analysis of UWC-3 standard (d13C = -0.91‰ V-PDB, Kozdon et al., 2011) bracketing samples is on average 0.7‰ (± 2 SD).
DOI: 10.13130/rd_unimi/n9enq4/levtxn
title: force_disp_init-136.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.967640
title: d13C values measured by Secondary Ion Mass Spectrometry in shells of the planktic foraminifer Morozovella velascoensis from ODP Site 865 (Central Pacific) across the PETM (~56 Ma)

description: Foraminiferal shells of the species M. velascoensis from sediments spanning ~650 ka across the PETM section of ODP Site 865, Central Pacific, were cast with 3 grains of UWC-3 calcite standard (Kozdon et al., 2009) in the center of a 25 mm round epoxy mount, ground to the level of best exposure, polished, cleaned, and Au-coated. Prior to geochemical analysis, shells were examined by Scanning Electron Microscopy (SEM) to identify subdomains suitable for in-situ d13C and Mg/Ca ratio measurements and to avoid diagenetically altered zones within each shell. In-situ d13C measurements were performed with ~7 µm beam spot size in the WiscSIMS Laboratory at UW-Madison by a CAMECA ims-1280 large radius multicollector ion microprobe) using the protocols described in a previous study (Kozdon et al., 2018). The in-situ d13C microanalyses primarily targeted subdomains located at the base of pustular outgrowths (muricae) along the chamber walls of each shell. Previous studies have shown that these subdomains are less susceptible to post-depositional alteration than the rest of the shell (Kozdon et al., 2011; Kozdon et al., 2013). Between one and five SIMS d13C microanalyses were performed for each shell. Reproducibility of the individual spot analysis of UWC-3 standard (d13C = -0.91‰ V-PDB, Kozdon et al., 2011) bracketing samples is on average 0.7‰ (± 2 SD).
DOI: 10.13130/rd_unimi/n9enq4/p2podx
title: force_disp_init-112.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/tkplt5
title: force_disp_final-120.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.954711
title: X-ray fluorescence measurements from Contessa Road (Italy)
DOI: 10.1594/pangaea.967638
title: Mg/Ca ratios measured by Electron Probe Microanalyzer in shells of the planktic foraminifer Morozovella allisonensis from the PETM section of ODP Site 865 (Central Pacific)

description: Foraminiferal shells of the species M. allisonensis from the PETM section of ODP Site 865, Central Pacific, were embedded in epoxy and polished to midsection. Suitable, well-preserved domains for in-situ analysis were identified by scanning electron microscopy. In-situ measurements of the Mg/Ca ratios were performed using a CAMECA SX-51 electron microprobe housed in the Cameron and Wilcox Microbeam Laboratory at the UW-Madison Department of Geoscience. Depending on the number of suitable targets for analysis, between one and seven Mg/Ca measurements were performed for each shell. Fully quantitative microanalyses (mineral standards, background subtracted, and matrix corrected) were performed using Probe for EPMA software (Probe Software, Inc.). The natural carbonate standards Delight Dolomite and Callender Calcite were used for Mg and Ca, respectively. Mg-K alpha X-rays were measured on two spectrometers and aggregated. Carbon was calculated within the matrix correction, being allocated as one atom of carbon to 3 atoms of oxygen, and oxygen by stoichiometry to the cations measured, thus analytical totals of 98 – 100.5 wt. % are a measure of accuracy. Analyses featuring analytical totals below 98 wt. % or above 100.5 wt. % were excluded from the data set
DOI: 10.13130/rd_unimi/n9enq4/upcise
title: nodes_init-103.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.967375
title: New splice for the late Pliocene interval ODP Hole 145-883C

description: Here we present new splice for the late Pliocene interval site 883 hole C. The composite depth scale was created by visual correlation of the shipboard gamma ray attenuation and porosity evaluator (GRAPE) wet bulk density (WBD) measurements between 883B and 883C starting at core 9H and ending at 18H. 883B 11H-1 0–57 cm, 883B 12H-1 0–10 cm, 883B 15H-1 0–20 cm, 883C 15H-1 0–5 cm were not considered in the correlation exercise because the recovered sediments had sidewall cave-in characterized by pebbles typical of the overlying Pleistocene sediments. In almost all cores, recovery was &gt; 100%. To account for this in terms of depth, cores with &gt; 100% recovery were compressed uniformly and fixed to the top drill log depth (depth mbsf) assigned to that core. Subsequent correlation of cores between holes B and C revealed apparent gaps in recovery. Cores were further uniformly compressed to account for the unrecovered sediments and a composite stratigraphic section was stitched together by switching between the two holes. On average, cores were compressed 17% and at most by 28% of their drilled depth (9.5 m). GRAPE WBD from 883B and 883C was then correlated to the composite section to generate tie points for each core to the composite section. The result of this exercise is a composite section of comparable depth to the driller's shipboard depth scale (109.4 meters below sea floor vs. 108.3 meters common depth) that accounts for all the major stratigraphic features present in the GRAPE WBD profiles of 883B and 883C Depth mbsf can be converted to depth MCD using two methods, depending on preferences. The first is to convert all your depth mbsf values to depth mbsfc. To do that, one must go to the site 883 initial report and compress all the cores by the amount of core expansion greater than 9.5 m (i.e., &gt; 100%). One can then use the splice tiepoints to convert from depth mbsfc to depth mcd that are listed in the table. The advantage of this approach is that you only have to interpolate the data from depth mbsf to depth mbsfc once. The other option is to go directly from depth mbsf to depth mcd. To do this, one will have to interpolate the data for each core of hole B and hole C seperately. The reason for this being that there is significant overlap between cores on the depth mbsf scale that were drilled in the same hole, so if one interpolates all the data from all the cores in hole B, for example, to depth mcd at once, one will notice in your data table that data from, for example, 883 B 17H section 7 is overlapping with data from 883B 18H section 1. This is obviosly wrong - the way to fix it is to use the mcd scale tiepoints from each core seperately rather than all together.
DOI: 10.13130/rd_unimi/n9enq4/alwmpe
title: edges_final-110.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/n0i5ex
title: force_disp_init-120.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.948506
title: Calcifying phytoplankton standing stocks in the North Pacific from the R/V Kilo Moana cruise KM1712

description: This dataset compiles the CaCO3 standing stocks of living coccolithophores (mg/m³), of detached coccoliths (mg/m³) and the integrated CaCO3 standing stocks of coccolithophores (mg/m²). The samples were collected in the North Pacific between Hawaii and the Gulf of Alaska during the R/V Kilo Moana cruise KM1712 in August 2017, with rosette Niskin bottles equiped with CTD (Sea-Bird SBE 9) at different depths throughout the photic zone including the deep chlorophyll maximum. To estimate the CaCO3 contribution by coccolithophore assemblages in each sample, we carried out the transformation of coccospheres in number of coccoliths, following the estimates by Yang and Wei (2003), and then we adopted the coccolith mass estimates by Young and Ziveri (2000). The coccolith mass of Noëlaerhabdaceae also took into account the estimates by Beuvier et al. (2019) considering different mass for E. huxleyi calcification degree.
description: Jess F. Adkins and William M. Berelson were chief scientists of the Kilo Moana cruise KM1712. Patrizia Ziveri and William R. Gray designed the sampling strategy. Alessandro Incarbona and Michaël Grelaud estimated the coccolithophores and coccoliths CaCO3 standing stocks.
DOI: 10.13130/rd_unimi/n9enq4/otvzum
title: edge_data_final-107.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/d12pgs
title: nodes_final-135.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/m6eqkj
title: edges_init-149.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.971078
title: Major and trace elements in sediments from Deming Lake, MN, USA (2022-2023)

description: Sediment samples from the lake bottom were collected from the boat in May 2022. Ten samples capturing a few centimeters depth of the upper sediment layer were collected from depths between 1 m and 16.5 m depth along a transect from the northern shore and slope of the lake using a Wildco Ekman dredge. Additionally, one gravity core was collected at 4 m depth that yielded seven discrete samples from depths between 0 and 7 cm into the sediment column. All sediment samples were transferred into acid-cleaned 50 mL centrifuge tubes aboard the boat and frozen on return from the field for transportation. These samples were subsequently freeze-dried on return to WHOI using a benchtop freeze dryer with a Polytetrafluoroethylene coated stainless steel collector (Labcono FreeZone). Once dry, each sample was ground to a fine powder using a FRITSCH Mini-Mill Pulverisette 23 with zirconium oxide bowl and grinding balls. Approximately 50 mg of bulk sediment powders were weighed into Savillex Teflon reactors and digested in 2 mL concentrated HF + 1 mL concentrated HNO3. These samples were then sequentially dried down and digested in aqua regia followed by 1:1 concentrated HNO3:H2O2 to destroy organics. Samples were dried down, fluxed in concentrated HNO3, redried, and constituted in 5 mL of 2 % HNO3. Aliquots (&lt;1 %) of the sediment bulk digests in 2 % HNO3 were then taken, diluted, and analyzed for major, minor, and trace elements on the Thermo iCAP-Q ICP-MS at the WHOI Plasma Facility. Indium (In) was added to samples at a concentration of 1 ng/g prior to analyses to monitor and correct for instrument drift by normalizing to In intensities. Concentrations were calculated using a five-point calibration curve obtained by fitting of ion beam intensities measured for serial dilutions of a gravimetrically prepared multi-element standard. The relative standard deviation (RSD) for five measurements of each sample was ~10% on the iCAP-Q. The accuracy and precision of similar concentration measurements on iCAP-Q at WHOI have previously been determined to be ± 5-10 % (1SD) based on comparison with USGS reference materials AGV-1, AGV-2, BHVO-1, BHVO-2, BIR-1, and BCR-2 prepared and analyzed as unknowns during earlier runs (Jochum et al., 2016; Shu et al., 2017).
DOI: 10.13130/rd_unimi/n9enq4/cpdxg9
title: edge_data_final-102.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.940125
title: An updated age model for sediment core DSDDP 5017-1-A

description: The age model for this core was updated to the IntCal20 curve (for radiocarbon dates) using BACON age modeling software (https://cran.r-project.org/web/packages/rbacon/). The data span 160,000 years and describe changes in Dead Sea hydroclimate and the surrounding landscape.
description: The type of datum:yearofcollection = the year that the core was collected, which is used to constrain the core top age.uth: U/Th date on primary aragonite, from Torfstein et al. (2015).c14: radiocarbon date on terrestrial plant debris, from Kitagawa et al. (2017).tiepointG: tiepoint to dated outcrops of the Lisan Formation, from Goldstein et al., (2020).tiepointS: tiepoint to the Soreq Cave speleothem oxygen isotope record, from Goldstein et al., (2020).tiepointO: tiepoint to Northern Hemisphere summer insolation, from Goldstein et al., (2020).
DOI: 10.1594/pangaea.971079
title: Major and trace elements in snow and ice from Deming Lake, MN, USA (2022-2023)

description: A core of ice from the center of the lake was obtained in March 2023 using a Kovacs Mark V coring system. The core barrel extracts a 14 cm diameter ice core and returned a ~40 cm-long ice core topped with ~5 cm of snow cover. This core was transported back to the field station in a clean plastic bag. Visual examination of the core revealed the presence of 3 layers: a ~5 cm unconsolidated snow layer at the top; a ~20 cm opaque layer identified as deriving from snow and referred to hereafter as 'snow ice'; and a ~20 cm transparent layer identified as frozen lake water or 'lake ice'. The outer layer of the ice core was washed liberally with methanol and Milli-Q water prior to sampling, and all samples from the ice core specifically avoided the outer surface of the core that was in direct contact with the coring system. Five discrete sample layers, one from the unconsolidated snow and two each from the snow ice and lake ice, were collected from this core by manual separation with a ceramic chisel. These approximately 400 mL samples were melted in acid-cleaned 500 mL Savillex Teflon reactors prior to transportation back to Woods Hole Oceanographic Institution (WHOI). Elemental compositions were determined using a Thermo Fisher iCAP-Q inductively coupled plasma mass spectrometer (ICP-MS) at the WHOI Plasma Facility following 200 dilution of a 10 μL aliquot in 2 % HNO3. Indium (In) was added to samples at a concentration of 1 ng/g prior to analyses to monitor and correct for instrument drift by normalizing to In intensities. Concentrations were calculated using a five-point calibration curve obtained by fitting of ion beam intensities measured for serial dilutions of a gravimetrically prepared multi-element standard. The relative standard deviation (RSD) for five measurements of each sample was ~10% on the iCAP-Q. The accuracy and precision of similar concentration measurements on iCAP-Q at WHOI have previously been determined to be ± 5-10 % (1SD) based on comparison with USGS reference materials AGV-1, AGV-2, BHVO-1, BHVO-2, BIR-1, and BCR-2 prepared and analyzed as unknowns during earlier runs (Jochum et al., 2016; Shu et al., 2017).
DOI: 10.13130/rd_unimi/n9enq4/bgr3fg
title: nodes_init-146.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.960160
title: Data set for modeling methane fluxes of Beringian coastal wetlands

description: For upscaling CH4 flux estimates in Beringia during the past 20,000 years, we collected 231 present-day CH4 fluxes from coastal wetlands in the Northern Hemisphere. We combined our own flux data (27 plot measurements) from the Kenai Peninsula, Alaska with previously published data. Data were compiled from different sources (e.g. Treat et al. 2018; 2021; Poffenbarger et al. 2011; Liikanen et al. 2009; Holmquist et al. 2018; Kuhn et al. 2021). CH4 fluxes from the literature were calculated in g CH4 m-2 yr-1 for the growing season, which we set to 153 days (May to September). Each CH4 data entry was harmonized by classifying it into one of the six wetland types Saltwater, tidal regularly flooded, Temporarily irregularly flooded, Permanently to semi-permanently flooded, Seasonally flooded, Non-tidal saturated, Water-body. This resulted in a stratified pool of CH4 fluxes and allowed a bootstrapping approach to estimate uncertainty in the CH4 fluxes for Beringian coastal wetlands based on the variability of CH4 fluxes associated to the different wetland types. For each of 258 sites, the dataset includes a site description, calculated CH4 flux from this research, wetland type, wetland class, method of CH4 measurement, major vegetation type, site location, the originally published CH4 value ("orig val") in the referenced paper, original units of measurement, citation and persistent identifier for the original data source, and comments. For some of the data points no coordinates information was given in the original publication, therefore the latitude and longitude fields were left blank.
DOI: 10.13130/rd_unimi/n9enq4/9wkiru
title: nodes_init-148.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/tumxqt
title: edge_data_final-143.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/rfsssk
title: edges_init-141.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.13130/rd_unimi/n9enq4/s7l2m0
title: force_disp_final-104.dat

description: 250729_SIMULATION_DATA/TENS-M_1.zip
DOI: 10.1594/pangaea.960156
title: Methane flux measurements from coastal wetlands on the Kenai Peninsula

description: The methane (CH4) flux was measured during a field campaign in August 2021 on the Kenai Peninsula, Alaska. We chose locations in coastal wetlands along transects to cover a gradient from freshwater flooded into tidal, saltwater flooded wetlands. In total, we measured at 27 different locations including saltwater tidal regularly flooded bare grounds, temporarily irregularly flooded, as well as seasonally flooded, vegetated coastal wetlands.Flux measurements were made with a micro-portable LosGatos greenhouse gas analyzer (LosGatos Research) and a light-weight custom-made bucket chamber consisting of non-transparent PVC (diameter = 26 cm, volume ~ 19,000 cm3). We chose this small, lightweight equipment in order to be highly mobile in muddy, shrubby terrain and measure at field sites which were not easy to access. At each site we measured three replicates for 7 to 10 minutes, described the vegetation cover (if present), and measured the chamber and air temperature. The bucket chamber was equipped with a venting tube and a small fan to have well-mixed conditions in the chamber.The CH4 flux (in mg CH4 m-2 h-1) for each replicate measurement was calculated based on the volume and temperature of the bucket chamber, and the ideal gas law. We manually removed the first 30 sec of each measurement, because of potential disturbance while placing the bucket chamber on the site (we did not use pre-installed collars). Fluxes were calculated by applying a linear regression to the CH4 concentration and were given in mg CH4 m-2 h-1. The r squared was used to determine the quality of the linear regression. Fluxes that had a linear regression with a r squared below 0.9 were discarded. However, we did not want to exclude all the near-zero measurements as these indicate important data as well (no CH4 fluxes). Therefore, all measurements, which were below the precision of the greenhouse gas analyzer of 0.5 ppb (~0.44 mg CH4 m-2 h-1, depending on chamber volume) were included in the analysis as zero fluxes.In a final step, we averaged all the replicates from a measurement site in order to have one CH4 flux value per measurement site and calculated the CH4 flux for the growing season of 153 days in g CH4 m-2 yr-1, which served as input data for the bootstrapping of the Beringia coastal wetland CH4 estimation.