dataesr/scientific-paragraphs-categorization huggingface dataset:
5. Contralateral targeting was analyzed on P8. The data indicated that CPNs electroporated with the Epha4 plasmid projected to a larger target area (Figures  7F  and 7G ) and ectopically innervated the cingulate and motor cortices (Figures  7H-7O ). Overall, our results indicate that proper expression of EphA4 is required for CC axon targeting and that overexpression of EphA4 phenocopies target defects induced by miR-17-5p functional knockdown and PAE.
Finally, the refractive index of the brains was homogenized by immersion in dibenzyl ether overnight at RT. After imaging and 3D reconstruction on Imaris Software (v10. Oxford instrument), the dorsoventral distribution of electroporated axons was quantified on one coronal optical slice of clarified and 3D reconstructed brains at the level of the septum, fornix, and hippocampal commissure. The 10 longest tdTomato + axons in the contralateral hemisphere were traced from the midline using the FIJI NeuronJ plugin, and their lengths were measured. 51 alysis of electroporated brains at P8 P8 brains were fixed in 4% PFA in PBS overnight, sectioned with vibratome (VT1000S; Leica). and immunolabeled. Sections encompassing S1 and S2 were selected based on anatomical landmarks and DAPI staining, with reference to a developmental mouse brain atlas.
The contralateral innervation ratio was quantified by measuring the size of the contralateral projection area (from the position of the first tdTomato + axon observed from the midline in the contralateral cortex to the farthest). Values were normalized to the corresponding ipsilateral electroporated area (from the most lateral to the most medial electroporated neuron). To analyze the innervation in each cortical area, a threshold was applied to remove the background, and regions of interest (ROIs) corresponding to the different cortical areas were traced using Fiji-ImageJ. 92 The density of the tdTomato signal was measured in each ROI. Data were normalized to the density of the ipsilateral signal to avoid any differences due to electroporation efficiency.
Image acquisition Fluorescent images of vibratome and cryostat brain sections were acquired with an Apotome imager M2 (Carl Zeiss) equipped with a Hamamatsu C11440 digital camera or a Confocal LSM880 (Carl Zeiss) equipped with PMT, CH3, and GAasp photomultiplier detectors. Colorimetric staining was performed using the AxioImager M2 (Carl Zeiss) equipped with a CamColor camera or a LUMAR V12 Stereoscope (Carl Zeiss) equipped with a CamColor camera when a larger acquisition field was required. ZEN 2012 acquisition software was used for image acquisition on the Apotome and Confocal microscopes, and AxioVision software was used for image acquisition with the AxioImager and LUMAR microscopes. Images of whole brain slices were acquired as mosaics with 10% overlap and stitched together using ZEN 2012 software.
The images were transformed into TIFF format, processed, and quantified using ImageJ (ImageJ) and Adobe Photoshop 2019 software. Cleared brains were imaged using a light-sheet fluorescence microscope (Ultramicroscope II; LaVision BioTec) equipped with the ImSpector pro acquisition software. The sample and objective were immersed in a tank filled with dibenzyl ether to maintain a homogeneous refractive index between the specimen and objective. The sample was imaged in the coronal direction, and an image was acquired every 2. 5 mm, with bilateral illumination and a maximum gray level between 20,000 and 60,000 depending on the staining quality. The images were exported to the three-dimensional (3D) image processing software Imaris (Bitplane) to perform 3D reconstruction and then process the images.
Rotarod assay Adult (P60) control or PAE male mice were placed on a rod that slowly accelerated from 4 to 44 rpm over 5 min (rotarod apparatus; LSI Letica Scientific Instruments), and the latency to fall off the rod during this period was recorded. The test was performed on 3 consecutive days. Each day, the animals were tested three times, separated by at least a 5-min rest. Data were acquired on the last day. Complex wheel-running assay and tamapin injection Adult (P60) control or PAE male mice were housed in individual cages equipped with an activity wheel and an optical sensor to detect the number of wheel revolutions per time interval (Cat. # 80821S; Lafayette Instruments). Animals were first allowed to voluntarily run on a training wheel with all 38 rungs intact to become accustomed to the task.
After 10 days, the wheels were replaced by complex wheels with 16 rungs missing, according to the pattern shown in Figure  3B , and wheel-running activity was recorded for 1 week. The mice were treated with tamapin (Cat. # 10TAM001-00100; Smartox Biotechnology) administered at 15 mg/kg body weight via intraperitoneal injection every other day or with a control (saline) solution, and wheel-running activity was recorded for a week. Wheel revolutions were monitored at 1-min intervals using the Scurry Activity Monitoring Software (Cat. #80821S; Lafayette Instruments). The data obtained during the dark phase were analyzed. The total distance run, maximum velocity among daily runs, number of runs, and duration of runs were calculated. Fifteen PAE mice and 15 sex-matched control mice were tested.
Sequencing and analysis Librairies were generated using Illumina Stranded mRNA Prep with poly(A) selection and sequenced to at least 120 million mapped paired-end reads per replicate. In total, 73 bp paired-end reads were mapped to the mouse genome (mm10) using STAR (2. 7. 6a) with an average of 1. 24310 8 mapped reads (range, 1. 15 3 10 8 -1. 38310 8 ; standard deviation, 8. 45310  6  ). Mapped reads from individual replicates were assembled into transcripts using Samtools (version 1. 11) with default parameters. Differential expression was obtained using DESeq2 (version 1. 30. 1), which normalized the data by relative log expression. Data normalization had almost no effect on data distribution. A threshold of 1000 counts was applied before further analysis. miR-17 potential targets were identified using TargetScan version 7.
No samples or animals were excluded. All investigators were blinded to the treatment group during data collection and analysis. Each experiment was replicated a minimum of three times and data was reliably reproduced with each replication attempt. Statistical analyses were performed using GraphPad Prism version 6 or 9 (GraphPad Software, Inc. ). The normal distribution of the data was examined using the D'Agostino-Pearson omnibus, Shapiro-Wilk, or Kolmogorov-Smirnov tests.
ACKNOWLEDGMENTS The authors want to acknowledge the collaboration with  Dr. Gregor Kasprian  and his team at the  Medical University of Vienna, Department of Biomedical Imaging  and Image-guided Therapy. We thank  Francoise Muscatelli  (INMED) thank  Christophe Beclin  (IBDM),  Andrea Erni  (IBDM), and  Micaela Roque  ( IBDM ) for their advice and substantial help with the experiments. This work was supported by  Centre National de la Recherche Scientifique (CNRS), France ;  Aix-Marseille Universite, France ;  Institut National de la Santeet de la Recherche Medicale (Inserm ), France; and grants from  Agence Nationale de la Recherche (ANR)  ( WIRING-FASDBRAIN ,  ANR-18-CE91-0009 ) to F. M. The  France-BioImaging infrastructure is supported by the ANR  ( ANR-10-INBS-04-01 , '' Investissements d'Avenir' ').
Materials availability All renewable reagents generated in this study are available from the lead contact upon request. Data and code availability d The RNA-seq data have been deposited in the public functional genomics data repository Gene Expression Omnibus (GEO) and are publicly available as of the date of publication (accession number listed in the key resources table). d No unique code is described in this study. d All other data and any additional information required to reanalyze the data reported in this paper is available from the lead contact upon request.
Any long-term atmospheric pressure anomaly should be considered, at least for Holocene exposure periods  (Dunai, 2010). As such, we corrected the atmospheric pressure at the sampling sites by running the ERA40 atmosphere model  (Uppala et al. , 2005)  using the MATLAB function "ERA40. mat"  (Lifton et al. , 2014). We did not use the specific Antarctic atmosphere model  (Stone, 2000) , as the atmosphere in continental Antarctica is affected by the air flow over the ice sheet, and this modifies the elevation/air pressure relationship in the opposite way (cold high pressure at surface level). The difference between using the results obtained from the ERA40 model and the air pressure values from nearby weather stations (e. g. , Bellinghausen, 62. 2 S, 58. 9 W, 16 m a. s. l. ; 991. 05 hPa) is negligible, and thus the use of the ERA40 model in this area can be considered valid.
| Geochronological framework The dataset including 12 CRE samples provides ages spanning from 8. 1 ± 1. 1 to 1. 0 ± 0. 3 ka (Table  4 ). Exposure ages are generally consistent with the spatial distribution and geomorphological setting of the dated surfaces (Figure  3 ). Two samples collected from polished bedrock surfaces in the northern tip of the Fildes Peninsula reported CRE ages of 6. 2 ± 0. 9 ka (ART-32) and 8. 1 ± 1. 1 ka (ART-33), with a mean of 7. 2 ± 1. 7 ka (Figure  3 ). A similar average exposure age of 6. 6 ± 0. 9 ka was obtained from three erratic boulders distributed across the southern edge of the northern plateau: 7. 0 ± 0. 8 ka (ART-25), 6. 2 ± 0. 7 ka (ART-26) and 6. 8 ± 0. 9 ka (ART-25). A fourth sample that was dated at 4. 5 ± 0. 7 ka (ART-28) was identified as a potential outlier according to the chi-squared test (after  Ward & Wilson, 1978)  and therefore was excluded from the mean age calculation.
They also fall within the Neoglacial period and thus agree with the stratigraphic sequence. These Neoglacial advances were of reduced scope, but they provide information about the glaciation pattern across the area. More intense, colder conditions must have favoured a larger expansion of these glacial spots surrounding the plateau, which likely merged with the westwards expansion of the Collins Glacier, covering the entire northern sector of the Fildes Peninsula. Our results support this multiple-glacier spot model instead of a single independent ice cap that expanded or retreated according to prevailing climate conditions. However, we are cautious in this interpretation given the limited number of ages from the moraine, although the small number of dates is somewhat compensated for by the overall coherence of the CRE data, and we suggest that more data are needed to confirm this hypothesis.
ACKNOWLEDGEMENTS This research was funded by the  NUNANTAR (Fundação para a Ciência e Tecnologia of Portugal ;  02/SAICT/2017 -32002 ) and  CRONOANTAR (Ministerio de Economía y Competitividad, Spain ,  CTM2016-77878-P ) projects. Field research was also supported by the research groups  ANTALP  ( Antarctic, Arctic, Alpine Environments ;  2017-SGR-1102 ) funded by the  Agència de Gesti o d'Ajuts Universitaris i de Recerca of the Government of Catalonia  as well as by the  ZEPHYRUS (Climate Change and Environmental Systems) and College on Polar and Extreme Environments (Polar2E) of the Universidade de Lisboa. The study topics complement those of the project  NEO-GREEN  ( PID2020-113798GB-C31 ) funded by the  Spanish Ministerio de Economía y Competitividad. Marc Oliva  is supported by the  Ram on y Cajal Program  ( RYC-2015-17597 ) and  Marcelo Fernandes  by a PhD fellowship of the  Fundação para a Ciência e Tecnologia of Portugal  ( UIDB/00295/2020 ).
2. Place-based production and activation. Drawing from the creative outputs and discussions, the artists engaged in the design and development of multidisciplinary art outreach productions. The intent of these productions was to build on and express surfaced ideas of place, and respond to and activate notions of reclaiming space through public art. 3. Reflection and theorising. Throughout, the group engaged in reflection and participatory data analysis to capture and deepen meaning-making, and to explore theory building and knowledge mobilisation. Themes and findings emerging from this analysis formed a knowledge framework that continually informed as it was informed by new project cycles. The project cycles were facilitated by two white, cis-gendered female graduate students, identifying as queer (Phyllis) and heterosexual (Charlotte).
Acknowledgements We acknowledge with warm thanks and appreciation the many community artists, collaborators, arts workers, coordinators, and researchers who contributed hearts and minds to this deeply collaborative and evolving work. We specifically thank  Lisa Myers  for supervisory and curatorial support,  Leesa Fawcett  for helpful edits to this paper, and two anonymous reviewers for their insightful and generative feedback. We recognize the production partnership of SKETCH Working Arts, The Bentway and Artworks TO: Toronto's Year of Public Art. We are also grateful to have been supported in part by funding from the  Social Sciences and Humanities Research Council and FLIP Foundation.
At this stage, it is relevant to consider that in spite that the English word "computer" is meant to signify (programmable machine that can store, retrieve, and process data; Encyclopedia Britannica) the different Romanic languages retain the original meaning of computers as a person who either organizes or computes datasets  (e. g. , "ordinateur, ordenador, " in French and Spanish). In any case, we now universally use the term as meaning a device, usually electronic, that processes data according to a set of instructions. In this context, it is worth to remember that a more precise characterization of the computer was given early on by Mahoney in his historical review of computing in which the computer is being specifically defined as a fundamentally tripartite structure, which reflect the contributions of three historical disciplines concerned with the nature of this "machine/device" (electrical engineering; computer science and software engineering).
Acknowledgments We thank  Matthew Cobb  and  Alex Gomez-Marin  for critical reading of the MS. We also thank  R. Brette ,  M. Cobb ,  M. Chirimuuta ,  A. Danchin ,  C. Gershenson ,  A. Gomez-Marin ,  D. Graham ,  M. Levin ,  B. Richards ,  A. Roli , and  R. Solé  for feedback on resumes of their articles. Thanks are also due to  Marino Miculan  for clarifying a number of concepts in computer science. GM wishes to thank most warmly  Annalisa Pastore  and  Pierandrea Temussi  for valuable advice and constant encouragement.
Seismic reflection survey In 2007 in preparation of the TDP, more than 250 km of highresolution seismic lines (CHIRP) were acquired with an Edgetech tm 3200 with SB-424  (Russell and Bijaksana, 2012; Vogel et al. , 2015)  to characterize the sediment architecture of the basin and identify suitable sites for paleoclimate research. The data were acquired using a length of the source signal of 46 ms, a frequency of 3e15 kHz, and a shot time interval of 1 s, corresponding to shot spacing of approximately 1. 74 m. Coordinates were continuously recorded using a Furano tm GPS. The data were converted to SEG-Y files that were then imported into the seismo-stratigraphic interpretation software Kingdom 2020 provided by IHS Markit. No bandpass filters were used but small bulk shifts were applied prior to data visualization and export of the seismic sections.
, 2020)  for cores TOW6, TOW7, and TOW8. The R package CLAM v. 2. 3. 9  (Blaauw, 2010)  was used to generate age-depth models using a smooth spline interpolation. For core TOW9 we relied on the age-depth model presented in  Russell et al. (2014)  and for core Co1230 on the one presented in  Vogel et al. (2015).
In core TOW7 (Basin C), only 9 turbidites are observed with an average thickness of 15. 5 cm. Alternations coinciding with the occurrence of green or redsideritic clays are present across all petrophysical and geochemical datasets obtained for cores from Lake Towuti including TOW6, 7, 8, and 9 (Fig. 3 ) as well as Co1230  (Vogel et al. , 2015). Based on these major changes in lithology we suggest a sub-unit classification scheme for the upper ~10 m in the piston cores, based on the seismic and lithological unit classification introduced by  Russell et al. (2020b). For the purpose of correlating lithologies between the different basins and for core-to-seismic correlation, we rely mostly on the MS and GRAPE data. MS is elevated in red sideritic clay and low in the green clay lithologies  (Tamuntuan et al.
, 2015). MS therefore serves as an ideal dataset to correlate lithologies between the different cores and basins. GRAPE is particularly elevated in coarser/denser lithologies but also shows subtle changes at the transition of the fine-grained pelagic lithologies due to differences in sedimentary iron contents and interspersed sandy layers, often observed at the base of turbidites. GRAPE therefore serves as an ideal dataset to correlate turbidites between core and seismic data. Three lithostratigraphic Units L1a, L1b and L1c can be identified and correlated between cores TOW6, TOW7, TOW8, and TOW9 based on visual appearance and by matching prominent features of the MS data. The thickness of Unit L1a ranges from 113 (TOW7) to 240 cm (TOW9) in Basins B, C, and D, and reaches 640 cm thickness in the deep Basin A (TOW4 and Co1230).
8 ± 0. 64 ka. In unit L1c MS-based core-to-core correlation is hampered by the muted data variability and the lack of reliable radiocarbon dates in cores TOW 7 and 8. Sedimentation in Unit L1c appears fairly constant with estimated rates of up to 15 cm/ ka in all of the sediment cores. Therefore, we here focus on the last ~40 kyr BP where chronological constraints are most robust also due to the identified tephra marker layer, clearly visible in cores TOW6, TOW7 and TOW8, and dated to ~41 ka (Fig. 3 ). Sedimentation rates, calculated by considering turbidites as instantaneous (constant ages), vary between lithological units and cores from different basins. In contrast, Unit L1b shows a variable sedimentation rate, with a prominent peak in all cores but particularly pronounced in TOW9 with 35 cm/ka around 560 cm (~28.
Sediment core-to-seismic correlation In general, a strong correspondence between lithological and seismic facies is observed. This is particularly well demonstrated by the strong relationship of density with amplitude changes in seismic reflection data (Fig. 3 ). Low-amplitude reflections in seismic Unit S1. 1 coincide well with lithologic Unit L1a, which is characterized by green clays and infrequent occurrence of coarser turbidites or MTDs, as is also evident by the overall low density. Likewise, the transition between seismic Units S1. 1 and S1. 2 coincides with the lithological Unit L1a to L1b transition as it is characterized by an increase in amplitude and sediment density, respectively. Individual turbidites are clearly resolved in seismic data for cores TOW6, 7, and 8 where these deposits reach thicknesses of several decimetres.
Earthquakes as triggers of slope failure in Lake Towuti Available data for recent earthquakes on Sulawesi and more specifically for the vicinity of Lake Towuti, based on the USGS (Shakemap by USGS Earthquake Hazards Program; https:// earthquake. usgs. gov/earthquakes/eventpage/usp000huje/ shakemap/intensity) and IPE show 12 earthquakes with MMI ! VI (Supplementary Material Table  S2 ), sufficient to trigger sublacustrine slope failures  (Moernaut et al. , 2007; Van Daele et al. , 2015). As an example, the 2011 Mw 6. 1 earthquake with its epicenter 18 km to the north of Lake Towuti along the MF induced ground shaking with an intensity of VI along Towuti's northern shore (Fig. 2 ). In 1941, a Mw 6. 2 earthquake was recorded with an epicenter 8 km to the southeast of Lake Towuti, with an estimated MMI intensity of VII calculated on the shoreline.
S3 ) when applying the above-mentioned sedimentation rate. To better assess the return periods of earthquakes causing macroseismic intensities ! VI and !VII at the lake shore we used the IPE  (Leonard, 2015)  and earthquake events with Mw ! 4. 5 from the ISC catalogue, 2021. These data suggest return periods of ~8 years for ! VI and ~32 years for ! VII intensities, based on 12 events covering the last 100 years (Supplementary Material Table  S2 ). However, turbidites recorded in the cores of Lake Towuti are far less frequent compared to the number of earthquakes that can generate intensities ! VI at Lake Towuti. This is likely a result of insufficient sensitivity at Lake Towuti to record each individual seismic event with a triggered slope instability due to the overall low sedimentation rate in the different basins.
This is emphasized by the presence of frequent but rather thin turbidites at coring sites TOW6 and TOW9. In contrast, slopes are generally much more gently inclined in the southern Basins C and D (<4 ). This permits accumulation of a thicker sediment package over time that is less prone to failure. Turbidites in the southern basins are consequently less frequent but generally thicker than in Basin B (Figs. 3  and 9B ), as also evidenced by the presence of large slope failure related MTD's observed on seismic data (Fig. 6 ). Hence, the less frequent but thick turbidites suggest a lower sensitivity of slopes to fail during moderate earthquakes, and therefore imply a lower sensitivity to ground shaking. Consequently, we propose that high-intensity shaking is required to cause slope failures in the southern Towuti basins.
Acknowledgements This research was carried out with support from the  German Research Foundation (DFG)  and the  Swiss National Science Foundation, Switzerland (SNSF)  through grants awarded to  H. Vogel  (DFG:  VO 1591/2e1 ;  SNSF :  200020_188876  &  200021_153053 ) as well as through the  U. S. National Science Foundation (NSF)  through grants awarded to  J. M. Russell. Foreign research permits for field work at Lake Towuti were kindly granted by the  Ministry of Research, Education, and Higher Technology of Indonesia (RISTEK)  permit number  02/TKPIPA/FRP/SM/II/2010. Logistical support was kindly provided by  PT Vale Indonesia. We would like to acknowledge reviewers  Katleen Wils  and  Maarten Van Daele  who provided many helpful comments and suggestions which greatly helped to improve the manuscript.
, 2013; Zhao et al. , 2019). In addition, they do not allow partitioning the OH bias due to each precursor. In this context, the main objective of this study is to explore a simple approach to reconcile bottom-up and top-down estimates of the CH 4 sink by (i) improving the simulated atmospheric OH fields using multiple satellite observations and meteorological data from reanalysis and (ii) assessing the contribution of each main OH precursor to the bias in simulated OH and CH 4 sink. As a result, top-down estimates of CH 4 emissions will also benefit from the improved 3D distributions of OH  (Zhao et al. , 2020a; Saunois et al. , 2020). We first evaluate the OH precursors (CO, CH 4 , O 3 , CH 2 O, and NO 2 , the total column O 3 , and H 2 O (g) ) simulated for the year 2010 by the CESM1-CAM4Chem (Community Earth System Model using the Community Atmosphere Model version 4 as atmosphere component) and GEOSCCM (Goddard Earth Observing System Chemistry-Climate Model); these models participated in the CCMI-1 project, and they were used to estimate the global methane sink in  Saunois et al.