dataesr/scientific-paragraphs-categorization huggingface dataset:
Next, a state-ofthe-art reduction to the pole (RTP) filter was applied to the dataset, relocating the anomalies directly above their sources, to improve the interpretation of magnetic source locations relative to geologic features. The resulting RTP magnetic anomaly map (Fig. 5 ) displays geomagnetic field strengths ranging from 2950 to 3200 nT. Despite the removal of the long-wavelength IGRF, a SW-NE gradient is apparent. Various rather large magnetic anomalies are observed along the coast line and onshore in figure 5. These seem related to onshore tectonics/structures as the Pyrenean belt or the Nîmes fault for example. The largest magnetic anomaly observed is the CMA. Because of its amplitude, trend and location, and because we cannot associate it to known tectonics features, unlike the other anomalies, we decided to aim our study to understand the CMA and the anomaly B.
New Moho depth map A new map of Moho depth (Fig. 8 ) was computed during this study. The base map is an unpublished compilation (G. Martelet, pers. comm. )  of published data based on converted seismic interpretations in the GoL (e. g. Séranne, 1999; Gallart et al. , 2001; Mauffret et al. , 2001; Nercessian et al. , 2001; Gailler et al. , 2009; Moulin et al. , 2015). These data were complemented by Moho depths observed on passive seismic profiles by  Diaz et al. (2018)  in the eastern Pyrenees and by depths derived from the 3D model of  Wehr et al. (2018) , based on seismic interpretation and Bouguer anomaly constraints. The Moho depths calculated from the chosen model of this study were also taken into account. Moho isobaths, based on depths rounded to the nearest kilometre, were inferred from the structural configuration of the margin and the thicknesses of the synrift and postrift sediments  (Gorini, 1993; Guennoc et al.
, 1994; Séranne, 1999 ; Fig. 2 ). The most recent data were favoured, however, some areas where the connection between different datasets was not straightforward, we did not draw any isobaths especially between the Catalan and Roussillon basins (Fig. 8A , discussion below). The depth-to-Moho digital terrain model (colour field in Fig. 8A ) is computed by interpolation between the isobaths.
Acknowledgments: This study was carried out during the  OROGEN  project, funded by  TOTAL, BRGM , and  INSU-CNRS. We thank the  OROGEN's community  for their helpful discussions. We are thankful for the availability of the data accessible on the  European Marine Observation and Data Network Bathymetry portal  (http://www. emodnet-bathymetry. eu) for the bathymetric metadata and digital terrain model data products, and also for the  BRGM's InfoTerre portal  for the new geophysical compilation (the gravimetric and magnetic database). We thank  Andrew Alden  for his proofreading review, as well as the reviewers for their critical and constructive reviews.
Here, we review the first comprehensive dataset of calcification records from fossil shallow-water reef corals. It includes corals from 16 time-slices dated from 20. 8 to 1. 2 Ma that are in an excellent state of preservation and allow for the measurement of environmental proxy data (oxygen and carbon stable isotopes: δ 18 O, δ 13 C) and calcification variables (growth rate, skeletal bulk density, calcification rate). To account for temporal and regional SST and calcification trends, we use recalibrated stable isotope values and normalized calcification rates, and discuss possible driving mechanisms behind distinct under-or overcalcification  (hypo-and hyper-calcification). For a calibration of calcification performance relative to the optimum, we use a reference dataset based on recent reef corals from the Indo-Pacific (IP) and an independent validation dataset from the Western Atlantic and Caribbean (WA-C) that both include growth data from the optimal reef growth window and stressed environments (e.
The fossil dataset represents 16 geological time-slices being between 20. 8 and 1. 2 Ma old. It allows describing coral calcification patterns during the period of (1) the late stage of the transition from greenhouse to icehouse in the late Oligocene to middle Miocene (before ca 17 Ma), (2) the MMCO (ca 17 to 15 Ma) and Middle Miocene Climatic Transition (MMCT, ca 15 to 13 Ma) with the middle Badenian Salinity Crisis of the Central Paratethys (MBSC, 13. 8 Ma), (3) the beginning of the Northern Hemisphere Glaciation during the late Miocene and onset of the Messinian Salinity Crisis of the Mediterranean (MSC, 5. 6 Ma), and (4) the intensification of the Northern Hemisphere (NH) glaciation after 2. 9 Ma (Fig. 2 , Table  1 ). The majority of specimens belongs to the genera Porites (n = 34), Solenastrea (n = 21), Tarbellastraea (n = 9) and Orbicella (n = 5), whereas the genera Stephanocoenia (n = 2), Goniopora (n = 1), Siderastrea (n = 1), and Favites (n = 1) are of minor importance.
X-radiography Coral slabs were X-rayed with a digital X-ray cabinet (SHR 50 V). Density measurements were made using X-ray densitometry based on CoralXDS software (freeware)  (Helmle et al. , 2002). This method relies on the gray values recorded by X-radiographs from coral slabs (Plate S10-S16). Gray-scale calibration of X-radiographs (digital) to skeletal density is achieved by a process using X-radiographs from an aluminum wedge and aluminum plates having the same thickness as the coral slices for a background picture. Calibrations were checked and iteratively improved by measuring transects crossing the empty screen of the X-ray cabinet and a coplanar slice of massive aragonite having the same thickness as the coral slab to be measured (Fig. 3 ). Calibration standards were produced from micritic masses of Karlovy Vary travertine (Czech Republic) or shells of the large bivalves Tridacna and Glycymeris.
The Recent reference and validation datasets For a detailed evaluation of the calcification trends of z-corals from the late Cenozoic to the present-day, we use a reference dataset for the recent Indo-Pacific (IP) that we test with an independent validation dataset from the Western Atlantic-Caribbean (WA-C). In order to account for the heterogeneous dataset available from the Neogene and Quaternary, the reference and validation datasets were constructed so as to rely on separate biogeographic regions (IP vs. WA-C), different taxa of massive z-corals (Porites vs. Orbicella), and a set of distinct growth environments inside and outside the reef growth window as categorized in Table  1. The reference dataset is from data on the recent massive coral Porites spp. (with few data from Pavona and Platygyra) from the IP.
It is an extension of the classical dataset for the Great Barrier Reef (GBR) region  (Lough and Barnes, 2000)  through additional literature data from a variety of environments inside and outside the reef-window. It includes information from the tropics to the subtropical outposts of the global reef belt, from very shallow to deep (> 20 m) reef settings, from clear to turbid waters, semi-restricted (elevated salinity) vs. open-ocean environments, as well as from upwelling zones and volcanic CO 2 vents. This classification was kept as simple as possible in order to allow its use for fossil and recent corals in a compatible way (Table  1 ). In many cases, the sites of coral growth were classified into more than one category. Some factors known to have negative effects on coral growth (e. g. exposure to waves and storms) have not been included in the classification, because the information supplied on those factors in the literature is sparse, or even not available for fossil corals.
The validation dataset was constructed in an analogous way, from literature data on massive corals of the recent WA-C. This dataset also includes corals from a multitude of environments that were categorized as for the IP. In contrast to the reference dataset, it contains essentially data from Orbicella (in addition to Porites astreoides and Diploria). For every site of coral growth, IP and WA-C, literature data were averaged if measurements from more than one coral were available from one site to keep data consistent with the Lough and Barnes dataset  (Lough and Barnes, 2000).
Significance of sclerochronologies For this assemessment of calcification in scleractinian reef corals over the late Cenozoic, we do not present a review of the δ 18 O-sclerochronologies available, although significant contributions to paleoclimatology have been made, e. g. by the detection of NAO-type interannual climate variability in the Mediterranean region at 10 Ma  (Brachert et al. , 2006a). The main limitation for a significant result of a compilation is the very heterogeneous resolution of the individual sclerochronological datasets published. In this contribution, we provide three examples of sclerochronologies and discuss the problem of resolution for coral sclerochronological datasets together with extension rate effects on mean δ 18 O values. The examples were selected so that all have approximately the same geological age and represent a subtropical and tropical setting, respectively (Fig.
7 , Table  2 ). The two sclerochronologies from the subtropics derive from the same geological site but document discrepant seasonal SST contrasts of 6 °C and 9 °C, respectively (Table  2 ). We ascribe the difference in SST seasonality inferred from δ 18 O values to the different annual sampling resolution (samples yr -1 ) of the two records; datasets with a low number of samples per year (low extension rate; Fig. 7/A , Table  2 ) underestimate "true" seasonality, whereby no agreement exists in the literature about the resolution required for a reliable documentation of the seasonal SST cycle  (Leder et al. , 1996; Quinn et al. , 1996). An important aspect in this discussion is the type of record, i. e. whether a sclerochronological dataset shows a sinusoidal cycle or a "church window-type" pattern, because the latter is strongly biased to one of the two main seasons.
In the subtropical datasets, we document a "church window" pattern (Fig. 7/A, B ) which likely reflects that SSTs fell below the closing temperature of calcification during the cool season  (Mertz-Kraus et al. , 2009a; Mertz-Kraus et al. , 2009b). Thus, the cool season is underrepresented in the two sclerochronological records, and the difference in seasonal contrast between the two records is likely an effect of a different discrimination against the winter season by the low and high extension rate record, respectively (Fig. 7 /A, B, Table  2 ). In the tropical sclerochronology presented here, we document a sinusoidal pattern and an even lower seasonality (3 °C) than in both subtropical records, although the resolution of the dataset is very similar to that of the subtropical record with a low resolution (Fig.
9 ): negative relationships exist between extension rate and skeletal bulk density (R 2 = 0. 0931, p = 0. 01), and positive relationships exist between extension rate and calcification rate (R 2 = 0. 3398, p < 0. 001) and calcification rate and skeletal bulk density (R 2 = 0. 2955, p < 0. 001). With regard to averages per site, however, a significant positive correlation exists only between extension rate and calcification rate (R 2 = 0. 4552, p = 0. 01) whereas no statistically robust relationships exist between extension rate and bulk density (R 2 = 0. 1818, p = 0. 11) and bulk density and calcification rate (R 2 = 0. 1186, p = 0. 28), respectively. Taxonomic or site-specific calcification relationships were not tested because of the small numbers of specimens per taxon and/or site, except for Porites, which is the most common taxon in our dataset (46 %).
Evaluating calcification trends: reference and validation data from the Recent In cross-plots of the 3 calcification variables from the Recent reference and validation datasets, we identify a negative relationship for extension rate and bulk density, however, significant only in the IP (IP: R 2 = 0. 419, p < 0. 001; WA-C: R 2 = 0. 039, p = 0. 472), while extension rate and calcification rate display highly significant relationships in both, the IP and WA-C (IP: R 2 = 0. 908, p < 0. 001; WA-C: R 2 = 0. 699, p < 0. 001). A negative correlation between skeletal bulk density and calcification rate exists in the IP (R 2 = 0. 190, p < 0. 001), but not so in the WA-C (R 2 = 0. 115, p = 0. 06). Nonetheless, the.
9 ). As a result, the pooled reference and validation datasets allows accurate and consistent predictions of calcification rate to be made from any given extension rate (Equation (  1  (1) We do not use bulk density for making predictions of calcification rate in an analogous way, because uncertainty in the regression is higher due to more scatter in the data. Significantly, mean deviation of the measured values from those predicted by eq. (  1 ) for the IP is 0. 0 ± 0. 18 g cm -2 yr -1 for IP Porites and 0. 0 ± 0. 23 g cm -3 yr -1 for WA-C Orbicella, i. e. there is no measurable difference in predicted calcification rate between IP Porites and WA-C Orbicella. Qualitative effects of various environmental stresses on the calcification variables from recent and fossil corals are listed in Table  3  and shown in Figures  S3-S5.
Our findings fully reproduce the results of numerous single studies as reviewed by  Lough and Cooper (2011). Earlier studies showed that distance from shore (or exposure to waves) and pH variability in nearshore settings are also important variables for calcification traits on recent reef systems  (Crook et al. , 2013; Lough and Barnes, 2000; Scoffin et al. , 1992). However, these aspects were not recorded as single factors in the dataset because they were hard to infer systematically from the literature for individual growth sites and represent a mix of sediment turbidity and wave exposure, nutrient load and carbon cycling.
The calcification anomaly As a quantitative measure of calcification performance, we use a new approach that we term calcification anomaly. The calcification anomaly describes the difference between predicted (i. e. from a regression) and measured calcification rate for any given extension rate. A zero calcification anomaly equals optimal calcification within the reef window, while negative and positive anomalies are here termed hypoand hyper-calcification. As defined here, hypo-calcification (hypercalcification) has an effect on bulk density being lower (higher) than expected for any given extension rate. The regression equation used for making the predictions derives from the pooled datasets for the reef window environment (clear water) from the IP and WA-C (equation 1). In the reference and validation datasets, clear-water sites symmetrically plot around 0 (optimal calcification).
In the reference and validation datasets, clear-water sites symmetrically plot around 0 (optimal calcification) although the total spread exceeds ± 1 SD (Fig. 10 ). As predicted, subtropical sites also spread symmetrically around 0, however, hyper-calcified outliers exist. These outliers correspond to Platygyra daedalea and Pavona sp. In semi-restricted (elevated salinity) settings, Platygyra daedalea also forms hypercalcified outliers relative to Porites, albeit less extreme, likely due to a higher calcification potential than Porites  (Howells et al. , 2018). At volcanic CO 2 vents, calcification is optimal, although shifted towards positive values; at acidic and nutrient-rich freshwater seeps calcification performance is decreased. Deeper-water sites (> 20 m) show optimal calcification, likely because of high water clarity at the sites studied (Red Sea)  (Heiss, 1994).
Interestingly, corals from turbid environments display a large range of performances; while some sites display no effect of turbidity on calcification, it induces substantial reductions in others. Likely, this is a reflection of qualitative and quantitative differences in turbidity that were not recorded by the dataset  (Lough and Cooper, 2011). Upwelling of cold, CO 2 -rich water also has strong negative influence on calcification performance, however, records of optimal calcification have been found also in such settings and reflect variable degrees of upwelling intensity and Ω aragonite  (Manzello et al. , 2014). Hyper-calcified records are generally rare, but have been documented also in turbid and upwelling sites (single-specimen data only). However, in turbid water this is due to Platygyra daedalea having a higher calcification potential than Porites  (Howells et al.
Records of hyper-calcification are due to other taxa than Porites in the dataset. Hyper-calcification is not likely to occur in Porites/Orbicella, because optimal calcification will take place under optimal growth conditions, i. e. the reef growth window (Fig. 10 ). Hyper-calcification in the WA-C is essentially due to data from the southern Gulf of Mexico; it may reflect enhanced Ω aragonite due to evaporation in that region  (Cai et al. , 2010)  that is likely to enhance calcification of z-corals  (Kleypas et al. , 1999a).
The same is true for the water depth at the growth site that has no negative effect on calcification according to the calibration datasets (Fig. 10 ). The fact that our fossil dataset largely samples sites within marginal basins located rather close to shore with turbid water, or upwelling zones etc. (Table  1 ) implies that most negative calcification anomalies can be explained in terms of the cumulative effects of various, local stressors (Fig. 10 ). Nonetheless, hypo-calcification rather than optimal calcification was found also at clear-water sites, i. e. reef window-type environments (sites 2, 10, 14; Table  1 ). Although it is finally unknown whether hypo-calcification is due to too low density for a given extension or due to too low extension rate for a given bulk density (or a combination of both), it is more likely to reflect a too low bulk density for a given extension rate.
We come to this conclusion because modern z-corals display the lowest bulk density at sites having the lowest Ω aragonite , and these densities are significantly below those predicted from ambient SST  (Manzello et al. , 2014). Thus, biomineralization at low sea-water supersaturation with aragonite seems to promote investing calcification resources into extension at the expense of thickening and strengthening (i. e. bulk density)  (Mollica et al. , 2018). Neogene hypo-calcification at clear-water sites is, therefore, the likely expression of low pH and / or low Ω aragonite of open seawater. In this respect, it should be noted that one of the clear-water sites was classified also in the category "elevated salinity" (site 10; Table  1 ) (Fig. 10 ). Negative growth effects of evaporation and elevated salinity on calcification are not obvious in our reference dataset and were also not reported in the literature (Veron, 2011) (Fig.
10 ). This is an   1. interesting aspect, because hypersaline waters have a higher pH and Ω aragonite than the open ocean  (Kleypas et al. , 1999a). If these waters were not sufficiently supersaturated with aragonite to support moderntype calcification, reduced pH and carbonate supersaturation of the open ocean is a likely possibility for the time-slices dated 20. 8, 20. 3, 6. 5, and 2. 5 Ma (sites 1, 2, 10, 14, Table  1 ) and supports conclusions from independent proxy data  (Sosdian et al. , 2018). Over geological time (16 geological time-slices, plus Recent), calcification performance does not display a clear trend in our dataset, except for a minimum of the anomaly between 3 and 1 Ma and a maximum in the present-day (Fig. 11 ). Single-coral data at the 3 to 1 Ma calcification minimum display the highest degree of hypo-calcification recorded so far.
Conclusions 1 Fossil z-corals (n = 74) from 16 geological time-slices (20. 8 to 1. 2 Ma) were reviewed with regard to stable isotope proxies and calcification patterns. 2 Oxygen and carbon stable isotope data document for the most part marine growth environments consistent with subtropical positions in perennially arid and seasonally humid settings or upwelling. Intense evaporative signatures exist in corals from before the MSC in the Mediterranean and the MBSC in the Central Paratethys. 3 Coral sclerochronologies can significantly contribute to our understanding of paleoenvironments. However, low extension rates typical to fossil corals limits their intra-annual resolution and should be taken into account when comparing records of environmental variability, e. g. seasonal SST contrasts. 4 The newly introduced calcification anomaly is a quantitative measure of calcification performance that is independent of SST effects.
Acknowledgements Janice Lough  ( AIMS, Townsville, Australia ) generously shared with us her files on calcification in modern Porites (2013). Frank Bach  ( Leipzig University, Germany ) made fossil specimens from the " Felix Collection " available, and  Matthias Harzhauser  ( Natural History Museum, Vienna, Austria ) provided coral specimens from  Natural History Museum (Vienna, Austria ). The latter colleague is also thanked for his advice on the stratigraphy of the  Central Paratethys  and for supplying rare historical literature. Jarek Stolarski  ( Polish Academy of Sciences, Warsaw, Poland ) is thanked for his discussion on scleractinian microstructures. We thank an anonymous reviewer and  André Strasser  ( Fribourg University, Switzerland ) for their constructive and thoughtful suggestions to improve the manuscript.
5‰. More recently,  Meier et al. (2016)  analyzed the Hg elemental abundance and isotopic composition of a larger set of meteorites and found surprisingly large isotopic variations of both MDF (expressed as δ 202 Hg, the permil deviation of the 202 Hg/ 198 Hg ratio compared to the NIST SRM 3133 standard) and odd-MIF compared to that which was originally identified in  Lauretta et al. (2001) , consistent with earlier data reported in an abstract  (Wiederhold and Schönbächler, 2015). This work shows that carbonaceous chondrites exhibit odd-MIF signatures while non-carbonaceous chondrites do not. However, these measurements were limited to a few LL ordinary chondrites and a single L ordinary chondrite, and no enstatite chondrites were examined for a MIF signature. In addition,  Meier et al. (2016)  argued that the Hg isotopic composition of chondrites is lighter (δ 202 Hg down to -7.
Mercury concentration measurement Mercury concentrations in meteorite and rock samples were measured using a Lumex Hg analyzer RA 915F equipped with a pyrolysis attachment PYRO-915+. The instrument detection limit of Hg is 0. 5 ng/g. CRM GBW07311 and CRM GBW07405 were used to verify the data accuracy, with the determined concentration within ±10% of their certified Hg values. The Hg concentrations of samples were compared with those obtained from the multi-collector inductively-coupled-plasma mass-spectrometer (MC-ICP-MS) to evaluate and guarantee the Hg recovery (of 95±11%; 2SD) for all samples except for BV2 (82%), during the treatment (double combustions and trapping) and prior to isotope analysis (see below). The double combustion system consisted of a furnace quartz tube (25 mm OD, 22 mm ID, 1.
The sample solutions were introduced at 0. 7 mL/min, which gave an instrumental sensitivity of 2. 5 V on 202 Hg for 1 ng/mL Hg solution. Mercury concentrations of bracketing standards NIST SRM 3133 and secondary standard UM-Almadén were matched to the sample solutions within 10%. All samples were analyzed in three blocks with 33 cycles for each and within 10 min washout time in between samples to ensure the blank levels were <0. 2 % of the preceding sample signals. The data for mass-dependant fractionation of Hg isotopes is reported as δ x Hg, the permil deviation of the x Hg/ 198 Hg ratio relative to the NIST-3133 standard, and is defined as: / 198 Hg)sample /( x Hg/ 198 Hg)NIST SRM 3133 -1]× 1000 Eq. 1 where x refers to the mass of each isotope between 199 and 202 amu. By convention, δ 202 Hg is used for the discussion of MDF variations and as the reference ratio with which to calculate the mass-independent fractionation MIF.