dataesr/scientific-paragraphs-categorization huggingface dataset:
Brachiopod shells clumped-isotopes: an alternative paleothermometer? Although there is a strong correlation between our new Δ47 values from brachiopod shells and growing temperatures, Δ47 values at a given temperature are generally higher than what is expected from the state-of-theart equation of  Anderson et al. , (2021)  (Figure  4 ). This observation is in line with the results of  Bajnai et al. , (2018)  350 gathered in the CDES reference frame. To discuss modern brachiopod Δ47 on a larger dataset, the data from  Bajnai et al. , (2018)  were adjusted to the CDES 90 reference frame to better compare them with our data set in the I-CDES reference frame  (Bernasconi et al. , 2021). We acknowledge that the different standardisation protocols used   2021 ) equation, the latter being indistinguishable from the relationship derived from our new dataset (Figure  4A ).
We argue that the difference between the two datasets of modern brachiopod Δ47 may largely results from distinct taxonomic assemblages and/or sampled locations in both datasets. Indeed, our new Δ47 data from New Zealand brachiopods replicate very well with previous data from same brachiopod species and similar locations  (Bajnai et al. , 2018)  (see supplementary). The Δ47-temperature relationship derived using both brachiopod datasets,.
365 is still nearly within error of the equation of  Anderson et al. , (2021)  (Figure  4B ). The use of this latter equation to calculate brachiopod growing temperature results in a significant mean offset with environmental temperatures of ~ -3. 9 ± 1. 2°C (95% CI, Figure  4C ) for the combined brachiopod dataset. In consequence, based on the data available to date, we support the use the following brachiopod equation:.
Mg/Ca thermometer for brachiopod shells 380 Our Mg/Ca data obtained from the inner layers of brachiopod shells do not show any significant correlation with growth temperature (p=0. 94; Figure  1C , Table  3 ). Brand et al. (2013 Brand et al. ( , 2019) )  proposed that there is a strong correlation between the Mg/Ca molar ratio of brachiopod shell secondary layer and the growth temperature. However, they acknowledge that some species do not follow that trend they illustrated as the GBMgL. They suggest that such deviations resulted from either lower growth rate  (Brand et al. , 2013)  or higher ones  (Brand et 385 al. , 2019)  of the considered species relative to other brachiopods. This issue alone illustrates how from the largest dataset of modern brachiopods available so far (i. e. Brand's database), one cannot firmly determine whether or not Mg/Ca correlates with seawater temperatures.
We emphasize that our dataset lack brachiopod shells samples from equatorial surface marine waters (27°C <T< 32°C), which record the highest MgCO3 molar content in Brand's database  (Brand et al. , 2013 (Brand et al. , , 2019)). Interestingly, the highest MgCO3 contents reported by these authors were because: 1) Thecideide brachiopod shells are essentially made of primary shell fabric, secondary shell fabric (fibrous layer) being restricted to small areas of the shell such as the teeth and the inner sockets  (Williams, 1968 (Williams, , 1973)) ; 2) the primary shell layer has higher Mg/Ca ratios than the fibrous secondary layer in Rynchonellid and Terebratullid brachiopods  (Pérez-Huerta et al. , 2008; Gaspard et al. , 2018; Rollion-Bard et al. , 2019) ; 3) Ullmann The exclusion of Thecideida data from the data base published by  Brand et al.
Potential of other trace element/Ca proxy Our new, brachiopod Sr/Ca data show a significant weak negative correlation with ambient temperature (pslope < 420 0. 001; R² < 0. 40). This correlation is supported by a weak positive correlation between Sr/Ca and ∆ 18 Oc-w of the inner layers (pslope < 0. 01; R² = 0. 31) as we also expect Δ 18 O to decrease with increasing temperatures (i. e section 4. 1). However, it contradicts the pioneering findings  of Lowenstam, (1961) , which suggested a negative correlation between brachiopod shell Sr/Ca and ∆ 18 Oc-w. The brachiopod database of  Brand et al. , (2013)  shows no significant correlation between Sr/Ca and temperatures (pslope = 0. 20). Given the diverging conclusions from one dataset to 425 the other, Sr/Ca values of brachiopod shells do not appear to be controlled by growing temperatures, at the first order.
All but one Terebratulidine brachiopod shells are associated with "low" element/Ca ratios, while all but one Terebratellidine 455 brachiopod shells are associated with "high" element/Ca ratios; in line with trends in Sr/Ca ratios reported by  Ullmann et al. , (2017). Whether there is an environmental or a taxonomic control on trace element incorporation in articulated brachiopods remains unclear but data suggest there may be both. Higher element/Ca ratios were measured from Terebratella sanguinea (Leach, 1814) (Terebratellidina) than from Liothyrella neozelanica Thomson 1918 (Terebratulidina), while living in the same environment. Similarly, the Antarctic brachiopod 460 Liothyrella uva  (Broderip, 1833)  shows the highest Sr/Ca, Na/Ca and Li/Ca ratios, while belonging to the Terebratulidine.
It is worthy to note that in the dataset presented here, tropical samples are dominated by Terebratulidine brachiopods, while high-latitude samples are dominated by Terebratellidine brachiopods, which preclude confident testing of both hypotheses from this dataset. In the fossil record, differences in Mg/Ca and Sr/Ca ratios between brachiopod genera have been associated with different shell microstructures  (Ullmann et al. , 465 2020). Our new data do not support the use of the trace element/Ca ratios studied here as paleothermometers from a dataset of widely distributed and taxonomically diverse brachiopods. In other words, temperature is not the prime parameter that can describe trace element incorporation into articulated brachiopods from various environments.
475 The oxygen isotope fractionation equation presented here differs from other published equations including that of  Kim and O'Neil (1997). However, it is worthy to note that most brachiopod shell data  (Brand et al. , 2019, this study)  plot in-between thermodynamic equilibrium isotopic fractionation  (Daëron et al. , 2019)  and the equation of  Kim and O'Neil (1997)  (Figure  3 ). Deviation of brachiopod shell calcite δ 18 O from thermodynamic equilibrium (∆ 18 Oeq = δ 18 Obrach. calcite -δ 18 Oequilibrium) is obvious when we compare our data set to the equation of  Daëron et al. 480 (2019)  in the clumped isotope-oxygen isotope fractionation space (Figure  5A ) with most of our dataset showing higher Δ47 and lower δ 18 O than predicted (Figure  5B ), a feature previously highlighted by  Bajnai et al.
, (2018). As a result, brachiopod calcite shows apparent Δ47 and δ O temperatures respectively lower and higher than those predicted by the thermodynamic equilibrium. This deviation from equilibrium values has a Δ47-∆ 18 Oeq slope of 0. 019 ± 0. 005 in our new brachiopod dataset, indistinguishable from the slope 0. 017 ± 0. 003 reported by Bajnai et 485 al (2018) using δ 18 Osw from the δ 18 Osw database  (LeGrande and Schmidt, 2006). Brachiopod shell Δ 18 O data  (Brand et al. , 2003 (Brand et al. , , 2013 (Brand et al. , , 2019;;  this study) also highlight a large geochemical variability among brachiopods sampled from similar marine environment (T,S), with a Δ 18 O range often higher than 1‰ (Figure  3 ,  Brand et al. , 2019). Isotopic fractionation equations  (Brand et al. , 2013 (Brand et al.
, , 2019;;  this study) usually rely on Δ 18 Oc-w values plotted against mean annual temperatures. Thus, it would be tempting to attribute 490 such scattering of data to seasonal variations, in both temperature and δ 18 Osw, but only in the case of specimens that lived above or in the upper part of the thermocline. Such isotopic scattering is indeed expected if we consider datasets based on multiple sampling along the growth axis of an individual, such as in the case of  Brand et al. (2013; 2019). However, seasonal scattering in data resulting from intra individual geochemical variability is unlikely for our measurements performed on a large sampling area that should correspond to multiple months or 495 years of growth. For example, we note a great isotopic variability in both δ 18 O and Δ47 among the 9 specimens of Aerothyris kerguelenensis from Crozet islands even though the specimens were recovered from depths in the 105 to 355 m range with a narrow range of temperature (3-5°C) and salinity (33.
8-34. 2). These 9 samples, all collected from the shell inner layers from different individuals, records a Δ 18 O variability of 2‰, equivalent to a temperature range 500 of 8 to 10°C if interpreted as such, and Δ47 variability of 0. 02 ‰ equivalent to a temperature range of about 5°C. This subsample shows a significant Δ47-∆ 18 Oeq slope of 0. 027 ± 0. 007 (2σ; pslope< 0. 01 ; R²=0. 95, n=5), as well as a strong positive correlation between Δ 18 Oc-w and δ 13 C (pslope < 0. 01 ; R²=0. 69, n=9). These covariations most likely result from kinetic effects as defined by  McConnaughey (1989)  here recorded at the intra-specific level. The trends in these offsets within our new dataset, is similar to what has been reported from other brachiopod samples by  Bajnai et al. (2018).
520 Trace element incorporation into calcite can also be affected by kinetic effects  (Lorens, 1981; Busenberg and Plummer, 1985; Tesoriero and Pankow, 1996; Gabitov et al. , 2011 Gabitov et al. , , 2014)). Consequently, if kinetic effects have a strong influence on element incorporation into brachiopod calcite, we should also observe strong negative correlations of Sr/Ca, Na/Ca and Li/Ca ratios with ∆ 18 Oeq. We observe such significant correlations in the new dataset, in both the inner and outer layers' subsets (0. 40 < R² < 0. 55, p-slope < 0. 01), with a significant slope 525 change between the two subsets. The variation in element/Ca related to a similar variation in ∆ 18 Oeq as suggested by linear regression models, is about twice as high in the inner layers' subset than in the outer layers' subset.
Acknowledgments This study was founded by the  ANR-OXYMORE  (grant no. ANR-18-CE31-0020 ) The authors gratefully thank the leaders and teams of the N/O of the following expeditions: the  Walda cruise in S. E. Atlantic Ocean  ( Dr. M. Segonzac ,  IFREMER, Brest ); Sampling from Norway coasts (courtesy of the  Trondheim Biological station) ;  MD 30  "BIOMASS" around  Crozet Islands (Arnaud, Marseille, France  and  Prof.
, p(mean ΔT = 0) < 0. 001) 305 in both δ18 Osw hypotheses. On the other end of the spectrum, the equation ofDaëron et al. (2019), derived from slow growing calcite, overestimates brachiopod shells growing temperatures (Figure3, p(mean ΔT = 0) < 0. 001) in both https://doi. org/10. 5194/egusphere-2022-1144 Preprint. Discussion started: 4 November 2022 c Author(s) 2022. CC BY 4. 0 License. δ 18 Osw hypotheses. Although it lessens the accuracy of δ 18 O temperatures in this dataset, using the locally measured δ 18 Osw values over the salinity-based estimates improved their precision (4. 0 < 2σ < 5. 3 °C, n=13 rather than 5. 4 < 2σ < 6. 4 °C, n=18). Those two δ 18 Osw hypotheses regarding δ 18 Osw values have their own benefits and drawbacks.
for the two datasets could hamper the strength of this comparison. However, this comparison is supported by the good agreement between sample 143 from Bajnai et al. , (2018)  (Δ47 = 0. 670 ± 0. 008 ‰ CDES 90) and its replicate 355 sample Mv143b (Δ47 = 0. 664 ± 0. 006 ‰ I-CDES; Bajnai et al. , 2020; Fiebig et al. , 2021). Both datasets are first compared to the Anderson et al. (2021) calibration (Figure 4). Many brachiopod shells record higher Δ47 values than what is expected from the calibration of Anderson et al. , (2021) (Figure 4A-B), in line with the underestimation Δ47 temperatures relative to MAT when using this relationship (Figure 4C). The temperature-Δ47 relationship derived from the Bajnai et al. (2018) dataset appears significantly different from that of Anderson et 360 al. (.
530 and ∆ 18 Oeq in the multi-specific dataset. https://doi. org/10. 5194/egusphere-2022-1144 Preprint. Discussion started: 4 November 2022 c Author(s) 2022. CC BY 4. 0 License. The deviation from equilibrium isotpoic fractionation observed in the new dataset seems to be linked to either taxonomic or environmental factors. As observed when comparing the new data to the equation of Daëron et al. (2019) (Figure 3), deviations from equilibrium oxygen isotope fractionation are greater at lower temperatures, and more generally we observe more deviation from the equilibrium in high latitude environments than in tropical 535 environments. Around Crozet islands, the deeper the brachiopod lived the less deviation from equilibrium is recorded, both in oxygen isotopes and clumped isotopes. While we observe generally more deviation from isotopic equilibrium in Terebratellidina than in Terebratulidina in the whole dataset, the difference is not as striking as documented for trace elements.
Given the highly geographically biased distribution of the two suborders in the new dataset, this trend may be coincidental. However, several examples of Terebratellidine and Terebratulidine 540 living in the same environment show similar pattern. In Doubtful Sound (New Zealand) Terebratella sanguinea (Terebratellidina) deviates more from equilibrium isotopic composition than Liothyrella neozelanica (Terebratulidina) (This study,.
57 to 25. 30 mmol/mol, 0. 45 to 2. 05 mmol/mol, 3. 28 to 58. 47µmol/mol, and 1. 86 to 18. 28 mmol/mol, respectively (N=47). Sr/Ca show significant but weak negative correlations (0. 28 < R² < 0. 44; p-slope < 0. 01) with temperature. Li/Ca show significant and good negative correlations (0. 61 < R² < 0. 86; p-slope < 0. 001) with temperature, the strongest correlation (R²=0. 86) being reached in outer layers samples. Na/Ca show significant negative correlations (0. 38 < R² < 0. 60; p-slope < 0. 001) with temperature. Concentration of these three elements in brachiopod shells (Sr, Li and Na) are strongly positively correlated with each other (0. 66 < R² < 0. 93 for the whole dataset) especially while considering only https://doi. org/10. 5194/egusphere-2022-1144 Preprint. Discussion started: 4 November 2022 c Author(s) 2022.
3, a moderate correlation is between 0. 3 and 0. 5, and a strong correlation is above 0. 5. The error bars for these correlations were estimated following  63  The results of these tests, including their statistical significance and interpretation are described throughout the manuscript. To compare the CO 2 fundamental band center positions with laboratory data, we interpolated the latter to NIRSpec spectral resolution and fitted it with a single Gaussian as well. We stress that this fitting method is not meant to be representative of 7/15 the true molecular complexity, since band profile can get very complex, but rather to highlight a global trend in the shift of the band of CO 2 for different mixtures. Laboratory data of pure and mixed CO 2 were gathered from the LIDA database  64. Ice mixtures were prepared at low temperatures and then heated to the temperatures selected here to represent the variability between aphelion and perihelion temperatures.
Acknowledgements The DiSCo-TNOs team would like to thank  Weston Eck  and  Alaina Henry  of  STScI  for their help in preparing the observations for execution;  Bret Blacker  for his almost invisible and always helpful presence from submission to publication at the  STScI  office, and the Time Allocation and Executive Committees of the JWST because their generous effort and good work is essential for the scientific success of this impressive telescope. This work is based on observations made with the  NASA/ESA/CSA James Webb Space Telescope. The data were obtained from the  Mikulski Archive for Space Telescopes  at the  Space Telescope Science Institute , which is operated by the  Association of Universities for Research in Astronomy, Inc. , under  NASA  contract  NAS 5-03127  for JWST. These observations are associated with program #2418.
Phase 1: Literature Review Initial research included a targeted literature review of published qualitative studies in gMG to identify signs, symptoms, and functional impacts of gMG (search strategy contained within Supplementary Material Table  S2 ). A search of the PubMed biomedical database was performed in September 2020 using the following search terms: myasthenia gravis AND (qualitative research, interviews, narratives, focus groups, patient experience, grounded or phenomenological research, endpoint model, concepts, patient report, or self-report), limited to articles in English published in the last 10 years, and with an abstract available. Peer-reviewed qualitative research studies focusing on adult (at least 18 years of age) patient experience of gMG were included. Articles were excluded if they focused primarily on experience of treatment, pathogenesis, genetics, or molecular biology of MG (full list of criteria in Supplementary Material Table  S2 ).
Data Analysis Clinician Interviews Clinician transcripts were qualitatively analyzed using Microsoft Ò Excel Ò (Redmond, WA) to expedite the data analysis process. Feedback was categorized into themes, including establishment of gMG diagnosis in routine practice, description of a typical patient with gMG seen in practice, and followup and assessment of disease progression/disease control over time. Patient Interviews Interviews were audiorecorded with each patient's permission. Data from patient transcripts, including ratings of symptom bothersomeness or impact disturbance, were summarized using descriptive statistics. De-identified verbatim transcripts were analyzed using inductive coding techniques, where codes are developed from qualitative data and amended as themes emerge, and deductive coding techniques, where pre-existing codes are used to analyze data on the basis of established theories, as well as content and thematic analysis to identify patterns in the data using software specifically designed for qualitative analysis, MAXQDA Plus, V.
Conceptual Model of gMG Data arising from interviews were contextualized with evidence from the prior qualitative research findings of the literature review. Findings from all interviews were used to update and finalize the conceptual disease model of the patient experience of living with gMG  [25, 28]. This model is a visual representation of the daily experience of gMG, grouped by signs and symptoms, immediate impacts, and general impacts, which allows for a comprehensive understanding of the patient experience from both clinicians' and patients' perspectives to emerge.
Data Availability Qualified researchers may request access to study documents (including the clinical study report, study protocol with any amendments, blank case report form, statistical analysis plan) that support the methods and findings reported in this manuscript. Individual anonymized participant data will be considered for sharing once the product and indication has been approved by major health authorities (e. g. , FDA, European Medicines Agency, Pharmaceuticals and Medical Devices Agency), if there is legal authority to share the data and there is not a reasonable likelihood of participant re-identification. Submit requests to https://vivli. org/.
The majority of physical signs and symptoms related to muscle function impairments are covered when the three COAs are administered in concert, indicating good conceptual coverage of physical signs and symptoms related to muscle function impairment, which provides a comprehensive picture of gMG from the perspective of the patient (MG-ADL), substantiated with tests of patients' performance (QMG, MGC). Five of the 14 physical function impacts mentioned in the CE interviews are included (difficulty keeping the arm lifted, difficulty b Fig. 3   The patient population in this study was sufficient to meet the objectives; concept saturation was reached at the third round of interviews. It was diverse in terms of age (30-75 years old), time since diagnosis (less than a year to over 25 years), and education levels, thereby supporting the representativeness of these data to the wider gMG population.
Context. The recent Gaia Data Release 3 (DR3) represents an unparalleled revolution in Galactic archaeology, providing numerous radial velocities and chemical abundances for millions of stars as well as all-sky coverage. Aims We present a new chemical evolution model for the Galactic disc components (high-and low-α sequence stars) designed to reproduce the new abundance ratios provided by the General Stellar Parametriser-spectroscopy module for the Gaia DR3 and constrained by the detailed star formation (SF) histories for both the thick and thin disc stars inferred from previous Gaia releases. Methods. Sophisticated modelling based on previous Gaia releases have found evidence for narrow episodes of enhanced SF inferred in recent time. Additionally, Gaia DR3 indicated the presence of young (massive) low-α disc stars that show evidence of a recent chemical impoverishment in several elements.
Results The proposed three-infall chemical evolution model nicely reproduces the main features of the abundance ratio [X/Fe] versus [M/H] (X=Mg, Si, Ca, Ti, α) of Gaia DR3 stars in different age bins for the considered α elements. Moreover, the most recent gas infall -which started ∼2. 7 Gyr ago -allowed us to predict accurately predict the Gaia DR3 young population which has experienced a recent chemical impoverishment. Conclusions. We extended previous chemical evolution models designed to reproduce APOGEE and APOKASC data in order to predict new Gaia DR3 chemical abundances. To this aim, we proposed a three-infall chemical evolution model to better trace both (i) the young population in Gaia DR3 with evidence of chemical impoverishment and (ii) the SF history from previous Gaia releases.
For this reason, in the stellar atmospheres, we can find insights into the processes that determined the formation and regulated the evolution of various components of our Galaxy. Hence, previous studies focused on Galactic archaeology have had to complement the intermediate Gaia data releases with chemical data from ground-based observations. However, ground-based surveys like the GALactic Archaeology with HERMES survey (GALAH;  Buder et al. 2021) , the Apache Point Observatory Galactic Evolution Experiment project (APOGEE;  Majewski et al. 2017; Ahumada et al. 2020; Abdurro'uf et al. 2022) , Gaia-ESO Survey  (Randich et al. 2022) , The RAdial Velocity Experiment (RAVE;  Steinmetz et al. 2020) , and Large Sky Area Multi-Object Fibre Spectroscopic Telescope (LAMOST;  Yu et al. 2021)  continue to have all the issues associated with biased samples, hampering observations from Earth.
Results In this section, we show the results of the new three-infall chemical evolution model introduced in Sect. 3 for α-elements. In Sect. 4. 1, we compare Gaia DR3 data with the previous twoinfall models regarding different chemical species. In Sect. 4. 2, the main features of the proposed three-infall chemical evolution in the [X/Fe] versus [M/H] (X=Mg, Si, Ca, Ti, α) plane are discussed. In Sect. 4. 3, we present results of the temporal evolution of the SF and other Galactic disc observables. In Sect. 4. 4, we compare the model predictions with Gaia DR3 data for different age bins. In Sect. 4. 5, we show the dilution signature present in Gaia DR3 massive stars.