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This data publication includes standard rock magnetic data related to concentration, coercivity and magneto-mineralogy versus depth from six sediment cores (M72/5-22GC3, M72-5-22GC4, M72-5-22GC6, M72-5-22GC8, M72-5-24GC3, M72-5-25GC1), collected at the Arkhangelsky Ridge in the Southeastern Black Sea during the marine expedition M72/5 of the German research vessel RV METEOR (in May 2007). The data are related to publications by Liu et al. (2018, 2019, 2020), Liu (2019) and Nowaczyk et al. (2012, 2013, 2018, 2021a, b). Sediment cores were recovered using gravity corers. For paleo- and rock magnetic analyses clear plastic boxes of 20×20×15 mm were pressed into the split halves of the generally 1 m long sections of the sediment cores. Data are provided as six ASCII files (.dat, one for each core) with metadata header, followed by 12 data columns and are decribed in the associated data description file (pdf).
This data publication includes standard rock magnetic data related to concentration, coercivity and magneto-mineralogy versus depth from twelve sediment cores recovered from the Arkhangelsky Ridge in the Southeastern Black Sea, German RV Maria S. Merian expedition MSM33 in 2013: MSM33-51-3, MSM33-52-1, MSM33-53-1, MSM33-54-3, MSM33-55-1, MSM33-56-1, MSM33-57-1, MSM33-60-1, MSM33-61-1, MSM33-62-2, MSM33-63-1, MSM33-64-1. The data are related to publications by Liu et al. (2018, 2019, 2020), Liu (2019) and Nowaczyk et al. (2012, 2013, 2018, 2021a, b). Sediment cores were recovered using gravitiy and piston corers. For paleo- and rock magnetic analyses clear plastic boxes of 20×20×15 mm were pressed into the split halves of the generally 1 m long sections of the sediment cores. Data are provided as 12 ASCII files (.dat, one for each core) with metadata header and are decribed in the associated data description file (pdf).
Sediment cores PC02, PC03, and PC04 were recovered during the ship expedition MR16-09 Leg 2 of Japanese RV Mirai in 2017 (Murata et al., 2017) using piston corers. For paleo- and rock magnetic analyses clear plastic boxes with a volume of 7 cm3 were pressed into the split halves of the generally 1 m long sections of the sediment cores. X-ray fluoresence (XRF) scans were performed with an Itrax XRF Corescanner (Cox Analytical systems) at Kochi Core Center, Japan (Hagemann et al. 2024). The downcore resolution was set to 5 mm, and the scans were performed with a Mo X-ray tube at 30 kV and 55 mA for a measurement time of 15 s. The Itrax X-ray beam was set to 0.2 mm × 20 mm. Measurements of low-field magnetic susceptibility (klf same as: k-bulk) and its anisotropy (AMS) were performed with an AGICO MFK1-A susceptibility meter. The principal AMS axes Kmax, Kint, and Kmin, the three axes of the anisotropy ellipsoid, were used to calculate the degree of anisotropy, as well as the shape factor of anisotropy. The frequency dependency of magnetic susceptibility was determined with an automated MAGNON Variable Field Susceptibility Meter (VFSM) by measuring magnetic susceptibility at different frequencies with logarithmically equidistant steps at a field amplitude of 250 µT. Susceptibilities of core PC02 samples were measured at 7 frequencies F from 375 Hz to 4775 Hz. Samples from cores PC03 and PC04 were measured at 5 frequencies from 475 to 4775 Hz. The frequency dependency Dk/Dlog(F) then was determined by linear regression of susceptibility k versus the decadal logarithm of frequency F. Values are given as decay rate in percent over one frequency decade (% / decade (F)) relative to the measurement at the lowest frequency. Thus, values obtained are negative. Measurements of the natural remanent magnetization (NRM) and of the anhysteretic remanent magnetization (ARM) were performed with a 2G 755 SRM long-core cryogenic magnetometer. ARMs were produced with a 2G660 single-axis alternating field (AF) demagnetizer using 100 mT alternating field and 50 µT static field. NRMs and ARMs both were stepwise demagnetized with the in-line 3-axes AF demagnetizer of the cryogenic magnetometer. AF steps for NRM: 0, 5, 10, 15, 20, 30, 40, 50, 65, 80, 100 mT. AF steps for ARM: 0, 10, 20, 30, 40, 50, 65, 80 mT. Iso-thermal remanent magnetizations (IRM) were imparted with a 2G 660 pulse magnetizer using 1500 mT for producing a saturation magnetization (SIRM) and -200 mT for remagnetization of the low-coercive fraction. Measurements were performed with a Molyneux spinner magnetometer. Data records were turned into time series by applying the age model for PC03 (Hagemann et al., 2024), correlating PC02 to PC03, and correlating PC04 to PC03 (back to 140 ka) and further using the PISO1500 paleointensity stack (Channell et al., 2009), paleomagnetic data from the Black Sea (Liu et al., 2020, Nowaczyk et al., 2021), and paleoclimatic data from Antarctica (Jouzel et al., 2007; Bazin et al., 2013) for reference for older core sections.
This data publication includes stacked paleomagnetic data, inclinations, declinations, and relative paleointensities, for the time interval 120 to 180 ka, comprising data from twelve sediment cores recovered from the Arkhangelsky Ridge in the Southeastern Black Sea; German RV Meteor expedition M72/5 in 2007: M72/5-22GC6, M72/5-22GC8; German RV Maria S. Merian expedition MSM33 in 2013: MSM33-51-3, MSM33-52-1, MSM33-54-3, MSM33-56-1, MSM33-57-1, MSM33-60-1, MSM33-61-1, MSM33-62-2, MSM33-63-1, MSM33-64-1. The data are also described in Nowaczyk et al. (2021). Sediment cores were recovered using gravitiy and piston corers. For paleo- and mineral-magnetic analyses clear plastic boxes of 20×20×15 mm were pressed into the split halves of the generally 1 m long sections of the sediment cores. Data are provided as six ASCII files (.dat, one for each core) with metadata header, followed by 12 data columns and are decribed in the associated data description file (pdf).
Sediment cores were recovered during the ship expedition of German RV Polarstern in 2016 (PS97) using piston corers. For paleo- and rock magnetic analyses clear plastic boxes of 20×20×15 mm were pressed into the split halves of the generally 1 m long sections of the sediment cores. In order to determine the direction of the characteristic remanent magnetization (ChRM), demagnetization results of the NRM were subjected to principal component analysis (PCA) according to Kirschvink (1980). The PCA also provided the maximum angular deviation (MAD) as a measure of the precision of the determined ChRM direction. ChRM declinations obtained by PCA were rotated around a vertical axis until the declinations of all samples falling into a circular window of 35° around the direction expected from a geocentric axial dipole (-72.9°) yielded a mean of 0°. ChRM data from core PS97-085-1 (-85-3) were tentatively tilted by +17° (-7°) around the EW axis in order to parallel the maximum in the inclination distribution with the inclination of a geocentric axial dipole field. The anhysteretic susceptibility K(ARM) is defined as the ARM intensity normalised by the static field used for producing the ARM. The anhysteretic susceptibility normalised by the low field bulk susceptibility K(ARM)/klf then is a magnetic grain size proxy with low (high) ratios indicating relatively large (small) magnetite particles. In order to discriminate samples being dominated by low-coercive minerals (magnetite, Fe3O4 and greigite, Fe3S4) from samples being dominated by high-coercive minerals (mostly hematite, Fe2O3), the S-ratio was calculated using S=0.5×(1-[IRM(-200 mT)/SIRM(1500 mT)]). S-ratios range from 0 to 1, with: dominance of magnetite/greigite: 0<<S≤1, and dominance of hematite: 0≤S<<1. As another grain size proxy the ARM intensity was normalised by the SIRM: (1000×ARM/SIRM) with low (high) ratios indicating relatively large (small) magnetite particles. The factor of 1000 is introduced in order to avoid small numbers. Relative paleointensity variations were estimated by three different proxies: slope of NRM vs. ARM of common demagnetization steps (slope(NRM/ARM)), NRM intensity demagnetized with 30 mT normalized with bulk susceptibility klf (pjk(30mT)), and NRM intensity demagnetized with 30 mT normalized with saturation magnetization SIRM (pjs(30mT)). Data records were turned into time series by correlation to dated reference records from Antarctica (Wu et al., 2021) and the Black Sea (Liu et al., 2021).
This data publication includes paleo and rock magnetic data from three sediment cores, MSM33-53-1, M72-5-22GC4, M72-5-25GC1, collected in the southeastern Black Sea during the marine expeditions M72/5 of the German research vessel RV METEOR (in 2007) and MSM33 of the German research vessel RV Maria S. Merian (in 2013). The data are supplement to Nowaczyk et al. (2020) and have already been described in Liu et al. (2018, 2019, 2020), Liu (2019) and Nowaczyk et al. (2012, 2013). The cores were sampled at intervals between 1.7 and 3.0 cm. Core M72/5-22GC4 was also continuously subsampled using u-channels. All material was subjected to detailed paleo- and rock magnetic analyses. As a main result the Laschamps geomagnetic excursion at around 41 ka could be revealed (Nowaczyk et al., 2012, 2013, Liu et al., 2020). This feature of the geomagnetic field was characterized by a short but full reversal and very low intensities of the Earth’s magnetic field. However, data is more or less compromised due to the post-depositional precipitation of the magnetic iron suphide greigite (Fe3S4), mainly depending on water depth of the coring sites. Provided data demonstrate the impact of greigite as well as the differences between discrete sample and u-channels (Nowaczyk et al., 2020). Data are provided as several ASCII files providing most relevant rock magnetic and paleomagnetic parameters, the age model as well as detailed information on the location, water depth, cruises and dates.
This dataset contains the paleomagnetic supplementary material to the article Kelder et al. (subm.), which presents a magnetostratigraphic correlation of Late Miocene lacustrine sediments based on multi-polarity greigite. The multi-polarity is visible in most thermal paleomagnetic results (Zijderveld diagrams) by antipodal high and medium temperature components, while only one magnetic component was visible in the alternating field demagnetization diagrams. Based on this complex behavior, a tailored demagnetization approach was developed to allow for reliable magnetostratigraphic dating of lacustrine sediments.The dataset includes demagnetization data from four drill cores located nearby Paks, Hungary. They were not oriented, meaning that only the inclination could be used for paleomagnetism. The measurements took place at the Paleomagnetic Laboratory Fort Hoofddijk in Utrecht University, The Netherlands. For details about the methodology the reader is referred to the methodology in Kelder et al. (subm).Three types of data are distinguished:• Thermal demagnetization results (.th files)• Alternating field demagnetization results (.af files).• Interpreted magnetic vectors for demagnetization files (.dir files)The .th, .af. and .dir files can be viewed with Notepad or similar programs, and analyzed via the Open Source platform Paleomagnetism.org (Koymans et al., 2016). The .dir files only exist for the cores PAET-30 and PAET-34, because these were interpreted in detail, while the material of the other cores (PAET-26, 27) were mainly used for rock magnetic purposes.Finally, an overview of the data files, abbreviations and sample codes is provided in the data description file.
This dataset includes paleomagnetic and rock magnetic analyses from four sediment cores collected on continental slope of Storfjorden (EG-02, EG-03, SV-04) and Kveithola (GeoB17603-3) trough‐mouth fans and two cores collected at the crest of the Bellsund (GS191-01PC) and Isfjorden (GS191-02PC) sediment drifts (NW Barents Sea). The dataset gave the opportunity to reconstruct variation of past geomagnetic field at high latitude for the last 22 kya and define the path of the virtual geomagnetic pole (VGP). Data are presented as two metadata table: one with definitions of the column heads and one with the core details; six tables with the data on the measured rock magnetic and paleomagnetic parameters and 3 tables with the results of data analyses and elaboration. List of tables is as follows: 1) Metadata: definition of columns heads; 2) Metadata: core details; 3) GS191-01PC: down-core variation of rock magnetic and paleomagnetic parameters [k (10E-05 SI); ARM (A/m); MDF (mT); NRM (A/m); MAD (°); Incl PCA (°); Decl PCA (°)] for Core GS191-01PC; 4) GS191-02PC: down-core variation of rock magnetic and paleomagnetic parameters [k (10E-05 SI); ARM (A/m); MDF (mT); NRM (A/m); MAD (°); Incl PCA (°); Decl PCA (°)] for Core GS191-02PC; 5) EG03: down-core variation of rock magnetic and paleomagnetic parameters [k (10E-05 SI); ARM (A/m); MDF (mT); NRM (A/m); MAD (°); Incl PCA (°); Decl PCA (°)] for Core EG03; 6) EG02: down-core variation of rock magnetic and paleomagnetic parameters [k (10E-05 SI); ARM (A/m); MDF (mT); NRM (A/m); MAD (°); Incl PCA (°); Decl PCA (°)] for Core EG02; 7) SV04: down-core variation of rock magnetic and paleomagnetic parameters [k (10E-05 SI); ARM (A/m); MDF (mT); NRM (A/m); MAD (°); Incl PCA (°); Decl PCA (°)] for Core SV04; 8) GeoB17603-3: down-core variation of rock magnetic and paleomagnetic parameters [k (10E-05 SI); ARM (A/m); MDF (mT); NRM (A/m); MAD (°); Incl PCA (°); Decl PCA (°)] for Core GeoB17603-3; 9) Cores Correlation: GS191-01PC depth (cm) and ARM (A/m) down-core variations for core GS191-01PC (master core); GS191-02PC depth (cm), GS191-02PC depth transferred to GS191-01PC depth (cm), ARM (A/m) down-core for core GS191-02PC and correlation tie points; GeoB17603-3 depth (cm), GeoB17603-3 depth transferred to GS191-01PC depth (cm), ARM (A/m) down-core for core GeoB17603-3 and correlation tie points; EG02 depth (cm), EG02 depth transferred to GS191-01PC depth (cm), ARM (A/m) down-core for core EG02 and correlation tie points; EG03 depth (cm), EG03 depth transferred to GS191-01PC depth (cm), ARM (A/m) down-core and correlation tie points; SV04 depth (cm), SV04 transferred to GS191-01PC (cm), ARM (A/m) down-core for core SV04 and correlation tie points; 10) Age model: age model for Core GS191-01PC; GS191-02PC; EG02; EG03; SV04 and correlation tie points; 11) NBS stack: paleomagnetic inclination, declination and RPI variations for NBS22.2k stack. In order to define high-resolution correlation between the cores the along-core variation of rock magnetic and paleomagnetic parameters (Sagnotti et al., 2011; Caricchi et al., 2018; Caricchi et al., 2019) have been integrated with the distribution of characteristic lithofacies (Lucchi et al., 2013), and the available age constraints (Sagnotti et al., 2011; Caricchi et al., 2018, Caricchi et al., 2019; Caricchi et al., 2020). Core to core correlation has been reconstructed by means of the StratFit software (Sagnotti and Caricchi, 2018), which is based on the Excel forecast function and linear regression between subsequent couples of selected tie-points. The data are presented as one Excel sheet with eleven tables and in tab-delimited ASCII format in the zip folder: 2022-028_Caricchi-et-al_data-txt.zip.
This dataset contains paleomagnetic data used to create the magnetostratigraphy of the Ugljevik section in Bosnia and Herzegovina (thesis by Karin Sant, 2018). It is the only outcrop known with the early, middle and upper Badenian sediments exposed in a continuous section.The dataset includes thermal demagnetization (.th files) and alternating field demagnetization (.af files) data from several partial sections (UG08, UG11 and UG13) together forming the full section (correlation figure is attached). The measurements took place at the Paleomagnetic Laboratory Fort Hoofddijk in Utrecht University, The Netherlands. The displayed AF measurements were performed in the per component setting. For further details about the methodology the reader is referred to the methodology in the thesis of K. Sant (2018).The .th and .af. files can be viewed with Notepad or similar programs, and analyzed via the Open Source platform Paleomagnetism.org: http://paleomagnetism.org/ (Koymans et al., 2016). An overview of the data files, abbreviation and sample codes is provided in the data description file.
This dataset includes updated versions of high-resolution age models derived from six sedimentary cores collected from the southwestern Svalbard margin. The dataset presented here represents a refinement of a previous version (Caricchi et al., 2020; 2022), achieved through correlation of the stratigraphic trends of the ARM/k parameter with the GICC05modelext timescale and the NGRIP record (Rasmussen et al., 2014). Additional refinement was obtained from newly acquired and recalibrated radiometric data, as well as from improved lithological constraints. The dataset enables the calculation of sedimentation rates during glacial and interglacial periods and during short-lived, widespread meltwater pulses and Heinrich-like events, thereby allowing the reconstruction of ice-sheet instability and meltwater events along the Svalbard–Barents Sea margin over the last 60,000 years.
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