cometadata/datacite-titles-descriptions-related-identifiers huggingface dataset:
DOI: 10.1594/pangaea.928020
title: M/S Silja Serenade (Helsinki-Stockholm) pCO2 underway measurements in 2019-12

description: Quality control:Measurements during calibration, cleaning, maintenance and low discharge have been removed.-----Flag system:A flag system is applied to the data. Good data that passes the flag control, gets the flag of 11111111. If the raw CO2 partial pressure (not calibration corrected) is out of boundaries (20-1200 ppm), the first digit changes to 9, i.e. if this is only abnormality, the flag would be 9111111. All flags and their boundary limits are listed in the table below.--Flag =&gt; Parameter =&gt; Lower boundary to Upper boundary91111111 =&gt; CO2_ppm_wet =&gt; 20 ppm to 2000 ppm19111111 =&gt; T equ =&gt; -1 °C to 30 °C11911111 =&gt; T tech =&gt; -1 °C to 30 °C11191111 =&gt; Salinity =&gt; 5 to 811119111 =&gt; Pressure =&gt; 0.9 to 1.111111911 =&gt; coeff_A/coeff_B/coeff_C =&gt; -50/0.9/-0.0001 to 100/1.3/0.000111111191 =&gt; SHEQ_flow_LPM/LICOR_flow =&gt; 1.0/50 to N/A/N/A11111119 =&gt; Visually inspected bad data-----Calculations:The CO2 molar fraction observed by the LI-840A is denoted as wet CO2 molar fraction (CO2_ppm_wet).--The molar fraction with respect to dry air is calculated as,CO2_ppm_dry = CO2_ppm_wet / (1 - H2O_ppt/1000),where H2O_ppt is the H2O molar fraction measured by the LI-840A.--For each calibration sequence every 4 hour, a 2nd order polynomial function is fitted to the observed and real molar fractions:CO2_ppm_dry_cal_cor = coeff_A + coeff_B * CO2_ppm_dry + coeff_C * (CO2_ppm_dry)^2Polynomial coefficients (coeff_A, coeff_B and coeff_C) are interpolated between the calibrations.--CO2 partial pressure in dry air is calculated as,pCO2_uatm_dry = CO2_ppm_dry_cal_cor * P_eq_atm--The CO2 partial pressure in wet air (Dickson and Goyet, 1994),pCO2_uatm = pCO2_uatm_dry * (1 - Pws_eq_atm)where saturation water vapor pressure, Pws_eq_atm, is calculated from equilibratortemperature, T_eq_degC (Wagner and PruB, 2002, Eq. 2.5).--Temperature corrected CO2 partial pressure is given for the inlet,pCO2_uatm_temp_corr = pCO2_uatm * exp [ A* (T_in_degC - T_eq_degC)]where A = 0.0423 (Takahashi et al., 1993).
DOI: 10.1594/pangaea.928022
title: M/S Silja Serenade (Helsinki-Stockholm) pCO2 underway measurements in 2020-01

description: Quality control:Measurements during calibration, cleaning, maintenance and low discharge have been removed.-----Flag system:A flag system is applied to the data. Good data that passes the flag control, gets the flag of 11111111. If the raw CO2 partial pressure (not calibration corrected) is out of boundaries (20-1200 ppm), the first digit changes to 9, i.e. if this is only abnormality, the flag would be 9111111. All flags and their boundary limits are listed in the table below.--Flag =&gt; Parameter =&gt; Lower boundary to Upper boundary91111111 =&gt; CO2_ppm_wet =&gt; 20 ppm to 2000 ppm19111111 =&gt; T equ =&gt; -1 °C to 30 °C11911111 =&gt; T tech =&gt; -1 °C to 30 °C11191111 =&gt; Salinity =&gt; 5 to 811119111 =&gt; Pressure =&gt; 0.9 to 1.111111911 =&gt; coeff_A/coeff_B/coeff_C =&gt; -50/0.9/-0.0001 to 100/1.3/0.000111111191 =&gt; SHEQ_flow_LPM/LICOR_flow =&gt; 1.0/50 to N/A/N/A11111119 =&gt; Visually inspected bad data-----Calculations:The CO2 molar fraction observed by the LI-840A is denoted as wet CO2 molar fraction (CO2_ppm_wet).--The molar fraction with respect to dry air is calculated as,CO2_ppm_dry = CO2_ppm_wet / (1 - H2O_ppt/1000),where H2O_ppt is the H2O molar fraction measured by the LI-840A.--For each calibration sequence every 4 hour, a 2nd order polynomial function is fitted to the observed and real molar fractions:CO2_ppm_dry_cal_cor = coeff_A + coeff_B * CO2_ppm_dry + coeff_C * (CO2_ppm_dry)^2Polynomial coefficients (coeff_A, coeff_B and coeff_C) are interpolated between the calibrations.--CO2 partial pressure in dry air is calculated as,pCO2_uatm_dry = CO2_ppm_dry_cal_cor * P_eq_atm--The CO2 partial pressure in wet air (Dickson and Goyet, 1994),pCO2_uatm = pCO2_uatm_dry * (1 - Pws_eq_atm)where saturation water vapor pressure, Pws_eq_atm, is calculated from equilibratortemperature, T_eq_degC (Wagner and PruB, 2002, Eq. 2.5).--Temperature corrected CO2 partial pressure is given for the inlet,pCO2_uatm_temp_corr = pCO2_uatm * exp [ A* (T_in_degC - T_eq_degC)]where A = 0.0423 (Takahashi et al., 1993).
DOI: 10.1594/pangaea.928023
title: M/S Silja Serenade (Helsinki-Stockholm) pCO2 underway measurements in 2020-02

description: Quality control:Measurements during calibration, cleaning, maintenance and low discharge have been removed.-----Flag system:A flag system is applied to the data. Good data that passes the flag control, gets the flag of 11111111. If the raw CO2 partial pressure (not calibration corrected) is out of boundaries (20-1200 ppm), the first digit changes to 9, i.e. if this is only abnormality, the flag would be 9111111. All flags and their boundary limits are listed in the table below.--Flag =&gt; Parameter =&gt; Lower boundary to Upper boundary91111111 =&gt; CO2_ppm_wet =&gt; 20 ppm to 2000 ppm19111111 =&gt; T equ =&gt; -1 °C to 30 °C11911111 =&gt; T tech =&gt; -1 °C to 30 °C11191111 =&gt; Salinity =&gt; 5 to 811119111 =&gt; Pressure =&gt; 0.9 to 1.111111911 =&gt; coeff_A/coeff_B/coeff_C =&gt; -50/0.9/-0.0001 to 100/1.3/0.000111111191 =&gt; SHEQ_flow_LPM/LICOR_flow =&gt; 1.0/50 to N/A/N/A11111119 =&gt; Visually inspected bad data-----Calculations:The CO2 molar fraction observed by the LI-840A is denoted as wet CO2 molar fraction (CO2_ppm_wet).--The molar fraction with respect to dry air is calculated as,CO2_ppm_dry = CO2_ppm_wet / (1 - H2O_ppt/1000),where H2O_ppt is the H2O molar fraction measured by the LI-840A.--For each calibration sequence every 4 hour, a 2nd order polynomial function is fitted to the observed and real molar fractions:CO2_ppm_dry_cal_cor = coeff_A + coeff_B * CO2_ppm_dry + coeff_C * (CO2_ppm_dry)^2Polynomial coefficients (coeff_A, coeff_B and coeff_C) are interpolated between the calibrations.--CO2 partial pressure in dry air is calculated as,pCO2_uatm_dry = CO2_ppm_dry_cal_cor * P_eq_atm--The CO2 partial pressure in wet air (Dickson and Goyet, 1994),pCO2_uatm = pCO2_uatm_dry * (1 - Pws_eq_atm)where saturation water vapor pressure, Pws_eq_atm, is calculated from equilibratortemperature, T_eq_degC (Wagner and PruB, 2002, Eq. 2.5).--Temperature corrected CO2 partial pressure is given for the inlet,pCO2_uatm_temp_corr = pCO2_uatm * exp [ A* (T_in_degC - T_eq_degC)]where A = 0.0423 (Takahashi et al., 1993).
DOI: 10.1594/pangaea.928024
title: M/S Silja Serenade (Helsinki-Stockholm) pCO2 underway measurements in 2020-03

description: Quality control:Measurements during calibration, cleaning, maintenance and low discharge have been removed.-----Flag system:A flag system is applied to the data. Good data that passes the flag control, gets the flag of 11111111. If the raw CO2 partial pressure (not calibration corrected) is out of boundaries (20-1200 ppm), the first digit changes to 9, i.e. if this is only abnormality, the flag would be 9111111. All flags and their boundary limits are listed in the table below.--Flag =&gt; Parameter =&gt; Lower boundary to Upper boundary91111111 =&gt; CO2_ppm_wet =&gt; 20 ppm to 2000 ppm19111111 =&gt; T equ =&gt; -1 °C to 30 °C11911111 =&gt; T tech =&gt; -1 °C to 30 °C11191111 =&gt; Salinity =&gt; 5 to 811119111 =&gt; Pressure =&gt; 0.9 to 1.111111911 =&gt; coeff_A/coeff_B/coeff_C =&gt; -50/0.9/-0.0001 to 100/1.3/0.000111111191 =&gt; SHEQ_flow_LPM/LICOR_flow =&gt; 1.0/50 to N/A/N/A11111119 =&gt; Visually inspected bad data-----Calculations:The CO2 molar fraction observed by the LI-840A is denoted as wet CO2 molar fraction (CO2_ppm_wet).--The molar fraction with respect to dry air is calculated as,CO2_ppm_dry = CO2_ppm_wet / (1 - H2O_ppt/1000),where H2O_ppt is the H2O molar fraction measured by the LI-840A.--For each calibration sequence every 4 hour, a 2nd order polynomial function is fitted to the observed and real molar fractions:CO2_ppm_dry_cal_cor = coeff_A + coeff_B * CO2_ppm_dry + coeff_C * (CO2_ppm_dry)^2Polynomial coefficients (coeff_A, coeff_B and coeff_C) are interpolated between the calibrations.--CO2 partial pressure in dry air is calculated as,pCO2_uatm_dry = CO2_ppm_dry_cal_cor * P_eq_atm--The CO2 partial pressure in wet air (Dickson and Goyet, 1994),pCO2_uatm = pCO2_uatm_dry * (1 - Pws_eq_atm)where saturation water vapor pressure, Pws_eq_atm, is calculated from equilibratortemperature, T_eq_degC (Wagner and PruB, 2002, Eq. 2.5).--Temperature corrected CO2 partial pressure is given for the inlet,pCO2_uatm_temp_corr = pCO2_uatm * exp [ A* (T_in_degC - T_eq_degC)]where A = 0.0423 (Takahashi et al., 1993).
DOI: 10.1594/pangaea.940566
title: Updated age model of IODP Site 321-U1338

description: Original data from:Drury, AJ et al. (2016): Evaluating climatic response to external radiative forcing during the late Miocene to early Pliocene: New perspectives from eastern equatorial Pacific (IODP U1338) and North Atlantic (ODP 982) locations. Paleoceanography, 31(1), 167-184, doi:10.1002/2015PA002881Original Pangaea entry (with incorrect age model): doi:10.1594/PANGAEA.856679This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation.
DOI: 10.1594/pangaea.941668
title: FD-EMI prospection data Japsand wreck

description: This dataset represents frequency domain Electromagnetic induction (EMI) data created by using electromagnetic waves generated in a transmitter and recorded in three receiver coils to create maps of electromagnetic subsoil properties at different sensing depths. A CMD Mini-Explorer by GF Instruments was used. The device consists of one transmitter and three receiver coils. The planes of the coils were oriented horizontally (horizontal coplanar - HCP). The distance between the transmitter and receivers are 0.32 m, 0.71 m and 1.18 m. The measurements were performed with 10 Hz sampling frequency. The area was covered by randomly walked W-E-orientated and N-S orientated tracks with an average spacing of about 0.5 m between the tracks. An RTK-GPS (Stonex S9i) was connected to the device using a fixed fibreglass rod at a distance of 2 m to the coils, minimizing the influence of the electronics on the data. The data was collected July 21st 2020, to image a 17th century wooden ship wreckage in the North Sea tidal flat area west of the island of Hooge(Germany) (Coordinates, geographic WGS84, are provided in the data list).
description: This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation.
DOI: 10.1594/pangaea.962323
title: Late Quaternary Sr-Nd-Pb isotope composition of the siliciclastic sediment fraction of the marine sediment core PS72/287-3 from Barrow Strait, Canadian Arctic Archipelago

description: The Sr-Nd-Pb isotope composition of siliciclastic sediments from the marine sediment core PS72/287-3 from Barrow Strait was analyzed to identify changing sediment provenances during the last deglaciation and the Holocene. Barrow Strait was blocked by the confluent Laurentide and Innuitian ice sheets during the last glacial period and is hence very interesting to study deglaciation processes in the Canadian Arctic. Varying Sr and Nd isotope ratios during the deglacial period suggest changing sediment sources probably related to ice sheet dynamics and sediment transport processes. After the deglacial period, radiogenic isotope ratios evolved less variable, indicating just slight changes in sediment provenance related to more stable environmental conditions during the Holocene. Sample preparation and radiogenic isotope analysis were conducted in the laboratories of the Isotope Geochemistry Group at MARUM – Center for Marine Environmental Sciences, University of Bremen, Germany. Sediment samples were leached using a NaOH-buffered solution of hydroxylamine hydrochloride and 15% acetic acid in order to separate the siliciclastic sediment fraction (adapted from Gutjahr et al. 2007, https://doi.org/10.1016/j.chemgeo.2007.03.021). Using a Thermo-Fisher Scientific TRITON Plus thermal ionization mass spectrometer (TIMS), the isotope ratios were determined after the elements had been separated by column chemistry.
description: This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation.
DOI: 10.25549/uschist-ouc110710750
title: Daily Trojan, vol. 39, no. 59, Dec 9, 1947

description: Southern California Daily Trojan, vol. 39, no. 59, December 9, 1947.
DOI: 10.1594/pangaea.965865
title: Mineralogical characterisation from XRD analysis of sediments and soils in the catchment of Lashmars Lagoon, Kangaroo Island (Karti/Karta), southern Australia

description: These data comprise XRD mineralogical analysis of twelve soil and sediment samples from the catchment surrounding Lashmars Lagoon, Kangaroo Island (Karti/Karta), southern Australia. To assess possible changes of sediment sources to Lashmars Lagoon over the past 7 kyr that could impact the interpretation of the palaeoenvironmental history of the site, these data were compared to the downcore XRD data from the composite lake sediment core (see 'Chronology, µXRF, XRD and bulk organic geochemistry from a lake sediment core from Lashmars Lagoon, Kangaroo Island (Karti), southern Australia, for the last 7 kyr'). The catchment soil and sediment samples were collected during field campaigns in November and December 2021. Soil samples were taken of the different surrounding surface geologies and sediment samples were taken from the creek inflows and one outflow to the lake, as well as a mudline sample from the northern basin of the lake. Mineralogy was determined by semi-quantitative XRD analysis using a Bruker D8 ADVANCE Powder X-ray Diffractometer with a Cu-radiation source operating at 40 KV and 40 amps, scanning 2 theta from 5 to 65 degrees with sample rotation of 30 rotations per minute. Data were interpreted using the software package DIFFRAC.EVA (Bruker, Karlsruhe, Germany) and Crystallography Open Database (www.crystallography.net/cod/) reference patterns for identifying mineral phases. Semi-quantitative estimates of mineral composition were obtained by Rietveld modelling using the program DIFFRAC.TOPAS 4.2 (Bruker, Karlsruhe, Germany).
description: This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation.
DOI: 10.1594/pangaea.967142
title: Field observation data in the Yangtze Estuary during Typhoon Muifa

description: The data includes pressure, sea pressure, and depth information of surface elevation. Field measurements have been collected from September 8th, 18:00, to September 15th, 18:00, for a total of 7 days in 2022 (China Standard Time, UTC+8). The study area is situated in Chongming Island, Shanghai. This region serves as a typical estuarine wetland in the Yangtze River Estuary. We set three observation points (121°56'12.988″E, 31°27'20.69''N; 121°56'2.5″E, 31°27'32.15''N; 121°56'.760″E, 31°27'33.95''N). During the observation period, from September 12th, 18:00, to September 15th, 18:00 2022, the hydrodynamics at the measuring points were affected by Typhoon Muifa. Chongming Island assumes a paramount role in safeguarding the ecological and environmental stability of the Yangtze River Delta region. Nevertheless, the island faces vulnerabilities, particularly in the face of natural disasters such as typhoon-induced storm surges during the summer season. A comprehensive examination of the typhoon events on the wave evolution within coastal wetlands holds substantial relevance. The implications of this research extend beyond localized defence strategies, with broader implications for the domain of coastal science and resilience, as it contributes to our understanding of the complex interplay between natural forces and coastal ecosystems.
description: This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation.
DOI: 10.1594/pangaea.967407
title: Leaf area index, fraction of vegetation cover and clumping index data obtained over the Honghe farm in northeastern China in 2019
DOI: 10.1594/pangaea.967409
title: High-resolution reference maps from the Honghe farm in northeastern China in 2019
DOI: 10.1594/pangaea.969541
title: A new helium isotope recored of the Paleocene-Eocene Thermal Maximum from ODP Site 198-1209 (S1)

description: The Paleocene-Eocene Thermal Maximum (PETM; around 56 Ma ago) is arguably the most intensively studied event of rapid greenhouse warming of the geological past. The duration and age of the PETM, however, remains vividly debated, limiting our understanding of the response of the Earth System dynamics to rapid warming. Here we present new extraterrestrial helium 3 (3HeET) data across the PETM at ODP Site 198-1209 (N Pacific) that document a drop in 3HeET fluxes from 0.56 ± 0.02 pcm³/cm²/ka ~1 Ma prior to the PETM to values of 0.37 ± 0.02 pcm³/cm²/ka before and after the PETM. Our 3HeET-based chronology, optimized through spectral analysis and orbital tuning, indicates a duration of 160±10 ka for the PETM body/core, consistent with previous 3HeET estimates from ODP Site 208-1266 (Walvis Ridge). The PETM started at the onset of a 100 ka eccentricity maxima at 56080 ka BP and ended abruptly during a marked decline in eccentricity at 55883 ka, providing strong support for an orbital trigger of both its onset and termination. The reevaluation of the 3HeET age models of the high paleo-latitude ODP Site 113-690 shows that the prominent sedimentary and carbon isotope steps at this site were controlled by obliquity instead of precession. Our revised chronology suggests that obliquity was also the dominant driver of the repeated drops to lower δ13C values during the PETM in otherwise precession-dominated low latitude sites, possibly reflecting the repeated destabilization of methane hydrate or permafrost carbon stocks at high latitudes.This dataset contains the grayscale reflectance logs obtained on core photographs for ODP Site 198-1209A, B and C, new records of helium isotope and non-carbonate fraction data for ODP Site 198-1209 and the reconstructed apparent 3HeET fluxes (FET), instantaneous sedimentation rates (ISR) and ages. We also report new bulk carbonate carbon and oxygen stable isotope data for ODP Site 198-1209 that are included in a compilation of published bulk carbonate data from the same site along with their corresponding 3HeET ages. We include a compilation of published benthic foraminifera carbon and oxygen stable isotope data for ODP Site 198-1209 with their corresponding 3HeET ages. We also report a compilation of Fe and Ca concentrations, stable isotope data measured on bulk sediment, planktonic and benthic foraminifera from ODP Site 113-690 that are reported against a revised 3HeET-based age model we developed for this site using published 3HeET data and a revised 3HeET flux of 0.42 ± 0.02 pcm³/cm²/ka and an age of 55916 ka BP for point F (169.05 mbsf).
description: This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation
DOI: 10.1594/pangaea.969545
title: A new helium isotope recored of the Paleocene-Eocene Thermal Maximum from ODP Site 198-1209 (S2)

description: The Paleocene-Eocene Thermal Maximum (PETM; around 56 Ma ago) is arguably the most intensively studied event of rapid greenhouse warming of the geological past. The duration and age of the PETM, however, remains vividly debated, limiting our understanding of the response of the Earth System dynamics to rapid warming. Here we present new extraterrestrial helium 3 (3HeET) data across the PETM at ODP Site 198-1209 (N Pacific) that document a drop in 3HeET fluxes from 0.56 ± 0.02 pcm³/cm²/ka ~1 Ma prior to the PETM to values of 0.37 ± 0.02 pcm³/cm²/ka before and after the PETM. Our 3HeET-based chronology, optimized through spectral analysis and orbital tuning, indicates a duration of 160±10 ka for the PETM body/core, consistent with previous 3HeET estimates from ODP Site 208-1266 (Walvis Ridge). The PETM started at the onset of a 100 ka eccentricity maxima at 56080 ka BP and ended abruptly during a marked decline in eccentricity at 55883 ka, providing strong support for an orbital trigger of both its onset and termination. The reevaluation of the 3HeET age models of the high paleo-latitude ODP Site 113-690 shows that the prominent sedimentary and carbon isotope steps at this site were controlled by obliquity instead of precession. Our revised chronology suggests that obliquity was also the dominant driver of the repeated drops to lower δ13C values during the PETM in otherwise precession-dominated low latitude sites, possibly reflecting the repeated destabilization of methane hydrate or permafrost carbon stocks at high latitudes.This dataset contains the grayscale reflectance logs obtained on core photographs for ODP Site 198-1209A, B and C, new records of helium isotope and non-carbonate fraction data for ODP Site 198-1209 and the reconstructed apparent 3HeET fluxes (FET), instantaneous sedimentation rates (ISR) and ages. We also report new bulk carbonate carbon and oxygen stable isotope data for ODP Site 198-1209 that are included in a compilation of published bulk carbonate data from the same site along with their corresponding 3HeET ages. We include a compilation of published benthic foraminifera carbon and oxygen stable isotope data for ODP Site 198-1209 with their corresponding 3HeET ages. We also report a compilation of Fe and Ca concentrations, stable isotope data measured on bulk sediment, planktonic and benthic foraminifera from ODP Site 113-690 that are reported against a revised 3HeET-based age model we developed for this site using published 3HeET data and a revised 3HeET flux of 0.42 ± 0.02 pcm³/cm²/ka and an age of 55916 ka BP for point F (169.05 mbsf).
description: This dataset has been carefully reviewed and curated in accordance with PANGAEA's exceptionally high quality standards. However, due to discontinued communication from the authors' side, it did not receive the usual formal approval by the authors and therefore lacks final scientific validation
DOI: 10.25549/uschist-ouc18870219
title: Daily Trojan, vol. 39, no. 70, Jan 7, 1948

description: Southern California Daily Trojan, vol. 39, no. 70, January 7, 1948.