The Acre drill site (7°43^′30.09^′′ S, 72°38^′57.44^′′ W) is located near oil exploration well 2-CDST-1-AC (Agência Nacional do Petróleo, Gás Natural e Biocombustíveis – ANP) in the Municipality of Rodrigues Alves (AC) (Fig. 3). The drill site is situated on private land on a terrace of the western bank of the Juruá River (Fig. 4), adjacent to the urban area of Rodrigues Alves and with road access through the BR-364 highway. Drilling equipment was mobilized from Mariana (MG) in southeastern Brazil, ∼ 4400 km to the east, and arrived in Rodrigues Alves on 29 May 2023. Drilling commenced on 16 June 2023, and on-site operations ended on 22 December 2023, with well abandonment. During most of this time, there was a full retinue of drillers (∼ 30 persons) and scientists (∼ 6–8 persons) on site.

Slimhole drilling was undertaken by GEOSOL SA using a Boart Longyear LF230 wireline diamond coring rig, 275HP, rated for 22.8 t maximum pull, with a chuck drive and 9 m rod pull. The first phase of drilling reached 40 m depth with PQ coring tools (core diameter of 8.3 cm), followed by borehole enlargement to 12.25 in. (31.1 cm) for 10 in. (25.4 cm) casing installation. PQ coring continued to a depth of 550 m, followed by borehole enlargement to 8.5 in. (21.6 cm) for 5.75 in. (14.6 cm) casing installation. PQ coring again continued to 746 m, followed by a reduction in diameter, with the final phase cored with HQ coring tools (6.3 cm) to the basal depth of 923 m.

Before and during drilling, outreach activities were performed to inform the local communities about the purposes of the drilling and to disseminate scientific information related to the goals of the TADP (see Sect. 5 for more details).

After each drilling run, the cores were delivered to the scientific team, which operated in two 12 h shifts (day and night). The cores were cut into sections of up to 150 cm, following standard protocols to accommodate core handling, scanning instrumentation, and archiving.

Each section was labeled, then sealed with end caps at both ends, using blue tape on the top cap and red tape on the bottom cap to indicate core orientation. The sections were cut using a handsaw for soft cores and a wet saw for more consolidated cores. Each section was then weighed and measured. During drilling, the scientific team performed basic sedimentological descriptions using core catcher samples and sampled for geomicrobiology, pore gases, and pore waters.

All on-site core and section data, as well as the lithological description and all on-site samples, were recorded in ICDP's mobile Drilling Information System (mDIS), and labels for the samples were printed directly out of the system. Furthermore, to follow FAIR principles (Wilkinson et al., 2016), mDIS automatically assigns a globally unique identifier – the International Generic Sample Number (IGSN) – to holes, cores, sections, and samples.

Sedimentological descriptions and core catcher sampling. A 5–10 g sample was taken from each core catcher and stored in a labeled plastic bag. A small fraction (∼ 1 g) was used for a preliminary sedimentological description (texture and composition) under a binocular microscope, applying the Folk classification system and using hydrochloric acid (10 %) to identify the presence of carbonate minerals. The remaining sample was stored and sent to the Institute of Geosciences at the University of São Paulo for preliminary luminescence analyses to characterize sand maturity and provenance.

Geomicrobiology sampling. A sample was collected every 20 m down to 200 m depth and approximately every 100 m below that, using a 1–3 cm core segment taken immediately after core retrieval. The surface of each sample was scraped with a sterile spatula to remove potential contaminants. For molecular analysis, ∼ 20 g of sediment was collected with a sterile spatula and preserved in LifeGuard Soil Preservation Solution. Subsamples were stored in 20 or 50 mL Falcon tubes at 20 or 4 °C until processing and were transported under ice to the laboratory in São Paulo.

Pore gas sampling. Pore gas was collected using a headspace approach. Samples were collected every 20 m down to 200 m depth and every 50 m below that, using a 1–5 cm whole round (WR) core slice immediately after core retrieval and above the segment used for pore-water sampling (see below). Each sample was placed in a labeled gas-tight bag, sealed with a manual heat sealer, and stored in a vacuum chamber for 30 min, followed by extraction of 5 cm³ (5 mL) of gas for analysis.

Pore-water sampling. Fifteen WR samples were taken approximately every 20 m, from 20 to 220 m depth, and then approximately every 100 m until 630 m depth, with core lengths ranging from 20 to 50 cm. The surface of each WR was scraped with a spatula to remove potential contamination from drilling fluids and sediment smearing in the borehole. The remaining sediment was placed into the pore-water extractor fitted with Whatman Number 1 filters. The assembly was placed in a manual hydraulic press, and gauge forces of up to 15 t were applied. Water was extruded into a clean plastic syringe and then dispensed from the syringe through a 0.2 µm sterilized polysulfone disposable filter into labeled 2 mL brown glass vials. Drilling mud samples were also collected from the mud-shaker as a reference for potential contamination, because groundwater extracted from local wells was used to make the drilling mud. Water samples were also collected from the Juruá River, local springs, shallow piezometers, and water wells of up to 80 m depth for comparison. Samples were shipped to USP in São Paulo for δ18O and δ2H analyses on a laser absorption spectrometer, model L2130-i, from Picarro.

Borehole logging was conducted in both cased and open-hole sections. After coring to 558 m depth, open hole logs were conducted to provide a stratigraphic framework for interpreting online gas analysis and core analyses, and to evaluate operational issues such as borehole conditions. The logging was executed using a slimhole wireline system (Mount Sopris Instruments), equipped with caliper, natural gamma, magnetic susceptibility, resistivity, sonic, and fluid temperature and conductivity probes. Magnetic susceptibility and resistivity were only acquired from 40 to 558 m depth due to the 10 in. (254 mm) conductor casing installed from 0 to 40 m. Drilling operational constraints (stuck pipe to 751 m, borehole collapse below this level; see the TADP Operational Report Sect. 4.1 for details) prevented open hole downhole logging below 558 m depth.

After installing 5.75 in. (146.05 mm) casing from 0 to 558 m, the full waveform sonic (FWS) tool was run to perform a cement bond log (CBL) to ensure proper anchoring of the casing to the wellbore.

Real-time gaseous hydrocarbon monitoring (CH₄, C₂H₆, C₃H₈, i-C₄H₁₀, and n-C₄H₁₀) was conducted during drilling using the ICDP Online Gas Analysis (OLGA) system, which employs a water-gas separator to mechanically extract gases dissolved in the drilling fluid (Erzinger et al., 2006; Wiersberg et al., 2020). The extracted gas was continuously transported through a plastic pipe to the analytical laboratory, which was located 15 m from the drilling fluid circulation system. Gaseous hydrocarbons were analyzed every 3 min using a field automatic gas chromatograph (GC-SRI Instruments 86105400) equipped with a flame ionization detector and a hydrogen generator, with hydrogen used as the carrier gas. Gas composition data were recorded at 3 min intervals and correlated with drilling depth using lag depth and penetration rate data. Instrument calibration was performed with standard gases of known concentrations (CH₄: 4870 ppm; C₂H₆: 258 ppm; C₃H₈: 200 ppm; i-C₄H₁₀: 99 ppm; n-C₄H₁₀: 102 ppm), all with uncertainties of < 2 %.

All drill cores and core catcher samples were shipped to the CSD facility at the University of Minnesota, Minneapolis, Minnesota, USA. Thirty-four scientists from seven different countries visited during a month-long period (August 2024) for initial core description, logging, scanning, and sampling.

All cores were first scanned on a Geotek MSCL-S multi-sensor core logger for loop magnetic susceptibility, natural gamma, p-wave velocity, gamma density, and electrical resistivity. The cores were then split lengthwise, creating a working half for sampling and an archive half for lithologic description and scanning. The split-core halves were photographed with a Geotek MSCL-CIS digital linescan imaging system and logged on a Geotek MSCL-XYZ multi-sensor core logger for high-resolution point magnetic susceptibility and color reflectance spectrophotometry.

A detailed visual lithologic description was made of the cores. In addition, approximately 5000 samples were extracted at varied intervals through the core sequence for more than 30 types of discrete analyses to be undertaken at collaborators' institutions. A partial list of these ongoing analyses includes geochronology (zircon U / Pb, quartz and feldspar luminescence, weathering (U–Th) / He, ¹⁰Be, ²⁶Al, paleomagnetism, bio-chronostratigraphy), biotic composition (pollen, phytoliths, diatoms, ostracods, mollusks), provenance (zircon U / Pb, quartz and feldspar luminescence sensitivity), environmental magnetism, mineralogy (bulk X-ray diffraction (XRD)), scanning electron microscopy (SEM) with energy dispersive X-ray spectroscopy (EDS), inorganic geochemistry (carbonate δ13C, δ18O, and clumped isotopes, X-ray fluorescence (XRF), Nd-Sr isotopes, Li-Si isotopes), and organic geochemistry (total organic carbon (TOC), bulk δ13C of organic matter (OM), biomarkers). Preliminary measurements have been completed for a subset of the samples and a subset of the analyses. We include brief descriptions of primary analytical methods and a summary of available analytical results.

Core lithologic description aimed to characterize lithofacies and stratigraphic architecture. Grain size, detrital composition, and sedimentary structures were recorded continuously along the core to establish a detailed facies classification. Facies associations were recognized through the identification of decimeter- to meter-scale grain-size trends and the repeated stratigraphic juxtaposition of specific facies types. Pedogenetic features, including structures and authigenic mineral phases, were documented in detail, along with the identification of recurring pedogenetic overprinting cycles. Trace fossil occurrences and assemblages were also described.

Based on the core descriptions, informal stratigraphic units were delineated according to multi-meter-scale trends in grain size and bed thickness, reflecting broader depositional cycles. Major bounding surfaces were identified and used to define the limits of these stratigraphic units, especially where they coincided with abrupt changes in detrital composition or the onset of distinct pedogenetic features.

Pollen. Over 1000 samples were collected for pollen analysis, focused on facies that were the best candidates for palynomorph preservation but also including the abundant paleosols that rarely preserve palynomorphs. The summary here is based on the processing of 305 samples following standard procedures (Traverse, 2007). The organic matter recovered following standard processing was mounted on 75 × 25 mm microscope slides. Each slide was scanned using a NanoZoomer N20 whole-slide scanner that digitizes 21 focal planes in each coverslip. These images will be the permanent digital repository of the slides and curated in the Smithsonian's long-term collections. The images were uploaded into OMERO (Open Microscopy Environment) (Allan et al., 2012), a client server environment for managing, viewing, annotating, and analyzing imaging data that are stored on a central server, with a database for the metadata and which can be accessed via a web browser anywhere in the world. The analyst uses those images to detect and identify palynomorphs. We used a two-step process to analyze the images: in the first step, the analyst detects where palynomorphs are in the slide and draws a region of interest (ROI) around the palynomorph. In the second step, the analyst classifies each ROI using a predefined dictionary. We used the morphological database of Jaramillo and Rueda (2025) to identify taxa, which includes all palynological publications from South America, and the biostratigraphic zonation of Jaramillo et al. (2025) to date the sequence.

Detrital zircon U / Pb geochronology. Thirty-two sandstone samples were collected along the drill core for detrital zircon (DZ) U-Pb geochronology, as well as samples from the modern sandbars of the Moa and Juruá rivers nearby the drilling locations to document modern age distributions. Zircon was separated from about 250 g of sandstone using conventional hydraulic and magnetic separation at the University of São Paulo. Zircon samples were mounted and analyzed at the University of Arizona LaserChron Center on the Nu instruments HR-MC-ICPMS (inductively coupled plasma mass spectrometer) coupled to a Photon Machines Analyze G2 excimer laser, using a rapid acquisition rate of 300 analyses h⁻¹ with a 30 µm spot size (Sundell et al., 2021). We utilized FC-1 as a primary standard, with SL and R33 as secondary and tertiary standards (Gehrels et al., 2008). Ages were filtered to retain only those with < 15 % analytical uncertainty. For grains younger than 900 Ma, ²⁰⁶Pb / ²³⁸U ages were used; for older grains, ²⁰⁷Pb / ²⁰⁶Pb ages were used. Additional filters were applied to exclude Proterozoic grains with > 30 % discordance or > 10 % reverse discordance. Maximum depositional ages (MDAs) were calculated for all samples using the maximum likelihood age algorithm (MLA; Vermeesch, 2021). Systematic and random uncertainties were propagated as detailed in Vasquez and Whiting (2005).

Luminescence dating and provenance. Forty-five samples for luminescence dating and 979 for luminescence provenance were collected for measurements at the University of São Paulo. First, optically stimulated luminescence (OSL) dating of quartz was tested in four samples from the upper 25 m of the core. Quartz and feldspar concentrates were prepared in the 180–250 µm fraction following standard procedures (Mahan et al., 2023). Quartz aliquots (100–300 grains) were measured for equivalent dose estimation using a single-aliquot regenerative dose (SAR) protocol (Murray and Wintle, 2003). Feldspar aliquots from samples at ∼ 4 m depth and ∼ 21 m depth were measured using a post-infrared infrared stimulated luminescence at 290 °C (pIRIR₂₉₀) SAR protocol (Buylaert et al., 2012). Radionuclide (U, Th, and K) concentrations were determined using high-resolution gamma ray spectrometry, and dose rates were calculated according to conversion factors by Guérin et al. (2011).

Luminescence measurements for sediment provenance analysis were carried out in polymineral aliquots (180–250 µm fraction) with the same volume. OSL sensitivity of quartz was measured according to Sawakuchi et al. (2018), which allows the discrimination of Amazonian sediments from Andean and cratonic sources. Quartz OSL sensitivity was measured after infrared stimulated luminescence (IRSL) to bleach feldspar signals. The quartz OSL sensitivity was calculated using the first second of light emission and blue stimulation (BOSL_1 s). The IRSL_1 s / BOSL_1 s ratio was used to evaluate the concentration of feldspar relative to quartz in the 180–250 µm fraction, which is a proxy for sand mineralogical maturity.

Heavy mineral analysis and provenance. A total of 160 samples was collected for the analysis of heavy minerals. Partial results were obtained from 26 samples in the lower half of the Acre drill core (505–915 m depth). To extract heavy minerals, the samples were wet-sieved to the 64–180 µm grain-size range, centrifuged in a low-viscosity polytungstate solution (LVP, 2.9 g cm⁻³), followed by freezing of the heavy minerals fraction and rinsing of the light fraction (Andò, 2020). Heavy mineral glass slides were prepared immersing the grains in Canada balsam for analysis under a polarized light microscope. Quantification is through the identification and counting of 150–300 non-micaceous transparent grains, employing the ribbon counting method (Galehouse, 1971).

Weathering (U - Th) / He geochronology. Four iron-enriched and one ferruginous laterite duricrust were sampled from weathered sediment outcropping in the vicinity of the drilling site and overlaying the Solimões Formation to complement geochronological data on 32 iron-manganese-rich pisoliths or strata from the drill core. For each sample, the material was split in half and photographed, and a subsample was selected for bulk mineralogical and geochemical characterization, as well as micrometric subsamples for (U–Th) / He geochronological analysis. Several aliquots weighing ∼ 50–150 µg were packed into Nd tubes and placed under vacuum for He analysis. Each Nd tube was degassed using a diode laser at temperature < 900 °C during 30 min to retrieve He content and after purification analyzed using a Prisma quadrupole. The tubes were then retrieved from under vacuum and placed individually into a Teflon savilex for wet chemistry digestion. Subsequently, the U, Th, and Sm contents were determined using an ICP-MS at the University Grenoble Alpes (France), using a protocol similar to that of Gautheron et al. (2021, 2022). In this way, the He, U, Th, and Sm content can be used to calculate the (U–Th) / He age for each aliquot with an analytical accuracy of ∼ 3 %.

Cosmogenic nuclides. Samples from the upper portion of the Acre core (∼ 22.7, 39.9, 50.8, and 74.2 m depths) were prepared for measurements of ¹⁰Be and ²⁶Al, targeting sediments that were presumed to record sediment deposition ages up to ∼ 5 Ma. Sample preparation included (i) sieving to acquire the 180–1000 µm fraction, (ii) magnetic separation using a Franz system, and (iii) hydrochloric acid (37 %) and oxygen peroxide treatments to remove carbonates and organic matter. These steps were performed at the University of São Paulo. Afterward, the samples were processed at the University of Potsdam (Germany). Quartz purification steps consisted of (i) heavy liquid separation (LST), (ii) seven rounds of 24 h and two rounds of 72 h in H₂SiF₆ : HCl solution, and (iii) one round of 24 h in HF 2 % solution and five rounds of 24 h in HF 1 % solution. The purity of quartz concentrates was tested using ICP-MS measurements. Then, the samples were dissolved in HF 40 % solution for 2 weeks. The HF was extracted, and the samples were dissolved in HCl for isotope fractionation. The isotopic fractionation of the samples is ongoing to isolate Be and Al fractions, with AMS measurements of ¹⁰Be and ²⁶Al to be completed at the Helmholtz-Zentrum Dresden-Rossendorf (HZDR) in Dresden, Germany.

Magnetic analysis. Magnetic susceptibility (MS) was measured by two independent methods: (1) along core sections using automated loggers and (2) on oriented individual subsamples. MS data were collected from WR core sections at 4 cm intervals and on the cores at ∼ 0.5 cm using a Bartington MS3 magnetic susceptibility meter coupled with a Geotek MSCL-S (whole core, MS2C loop sensor) and MSCL-XYZ (half core, MS2E point sensor) at the CSD facility. These values are expressed in 10⁻⁶ (whole core) and 10⁻⁵ (split-core) SI units. A total of 119 oriented cubic samples (8 cm³ each) were collected perpendicular to the core, primarily from fine-grained lithologies, such as mudstone and siltstone. These samples were obtained using non-magnetic knives and saws, stored in acrylic plastic boxes and analyzed at the University of São Paulo. The low-field MS of individual samples was measured using a Kappabridge MFK1-FA system (AGICO) at two frequencies: 976 Hz (low-frequency susceptibility; χLF) and 15 616 Hz (high-frequency susceptibility; χHF) in a 200 A m⁻¹ field at room temperature. The χLF and χHF were used to assess the behavior of magnetic grains throughout the χFD% parameter (χFD% = [(χLF - χHF) / (χLF × 100)]) (Dearing et al., 1996). All oriented samples were mass-normalized due to the irregular sample mass inside the cubic boxes, and MS data are expressed in m³ kg⁻¹.

Nd and Sr isotopic analyses. Samples of ∼ 1 g each were collected every ∼ 20 m (47 total). Samples were processed and analyzed at the University of São Paulo. Samples were first freeze-dried and wet-sieved (63 µm sieve), and then the < 63 µm fraction was centrifuged and oven-dried. The dried material was treated with 10 % HCl, rinsed, centrifuged, oven-dried, and ground with an agate pestle and mortar. Powder samples were dissolved by acid digestion, using HNO₃, HF, and HCl in Teflon beakers at 100 °C. Sr separation was performed using an Sr-specific resin and eluted with 0.05 M HNO₃. Nd was then separated from other rare earth elements first by using the RE resin and then an Ln resin. Sr samples were loaded on single tantalum filament with the addition of tantalum solution (TaCl₅). The ⁸⁷Sr / ⁸⁶Sr isotopic ratios were normalized to the value of ⁸⁶Sr / ⁸⁸Sr = 0.1194. Nd samples were deposited in rhenium parallel filaments with the addition of ultra-pure H₂O. Nd and Sr isotopic ratios were obtained by TIMS using a Thermo Triton. The ¹⁴³Nd / ¹⁴⁴Nd isotopic ratios were normalized to ¹⁴⁶Nd / ¹⁴⁴Nd = 0.7219 (DePaolo, 1981) and expressed in the εNd notation (Jacobsen and Wasserburg, 1980). Uncertainties in ⁸⁷Sr / ⁸⁶Sr and εNd refer to 2 SD and were calculated through multiple analyses. At this stage, 24 samples have been processed and analyzed for ⁸⁷Sr / ⁸⁶Sr and εNd, spanning the whole core and spaced ∼ 38.5 m from each other.

Inorganic geochemistry and mineralogy. We collected 837 samples of bulk sediment weighing ∼ 15 g each and spaced ∼ 1.1 m for magnetic, major elemental, and mineralogical analyses. Due to sample processing techniques, samples were first analyzed for magnetic properties (no sample treatment), then major elements (freeze-drying and grinding), and mineralogy (secondary milling), as described below.

For major elemental analyses, bulk sediment aliquots of ∼ 5 g were frozen at -60 °C, freeze-dried, and pulverized. The powder was pressed into Chemplex cups with attached thin Mylar foils. Analyses were carried out using a Malvern Panalytical Epsilon 1 X-ray fluorescence (XRF) spectrometer using the Omnian calibration at the University of São Paulo (USP), Brazil, following Kraft et al. (2025). To date, analyses have been completed for the upper 213 samples, representing the upper 267 m below the surface.

X-ray diffraction (XRD) analyses to characterize the qualitative and quantitative mineralogical composition of the sedimentary successions have so far been performed on 100 samples from the upper part of the well, down to a depth of 114 m. The analyses were performed using a Bruker D8 Advance diffractometer with CuKα radiation (λ = 1.54060 Å), operated at 40 kV and 25 mA, in collaboration with the Center for Mineral Technology (CETEM), Brazil. Samples pulverized for XRF were treated with a subsequent milling step using a McCrone mill to further reduce the particle size to below 10 µm, allowing for quantitative mineralogical analysis through Rietveld refinement with the fundamental parameters approach (Cheary and Coelho, 1992).

Diffractograms were acquired from randomly mounted samples using a step size of 0.02° and a scanning range from 4 to 105° 2θ. Qualitative phase identification was conducted using Bruker DIFFRAC.EVA v6 software, whereas quantitative mineralogical analysis was performed using Bruker DIFFRAC.TOPAS v6. Structures from the International Centre for Diffraction Data (ICDD) and the Crystallographic Open Database (COD) were used in the refinements. For general interpretation, minerals were classified into four main groups: (1) quartz, consisting solely of this mineral; (2) clay minerals plus mica, which include kaolinite, chlorite, smectite, and micas (such as muscovite, biotite, and illite); (3) feldspars, comprising K-feldspar and plagioclase; and (4) carbonates, including aragonite, calcite, and dolomite. Other phases comprise minor components, such as goethite and hematite.

Lithium isotopes. Lithium isotopic measurements (δ7Li) can be used to infer the history of weathering using the lithium (Li) isotope composition of the detrital sediment, based on a known relationship between chemical weathering intensity in river basins of the present-day Amazon and the isotopic signature of δ7Li in fine sediments. Forty-seven samples were collected throughout the length of the drill core and were collected in tandem with samples for Nd and Sr isotopic analysis as a constraint on provenance. Analyses are ongoing.

Organic geochemistry. Total organic carbon (TOC) and bulk organic carbon isotopic composition (δ13C) analyses were performed on 30 selected core catcher subsamples, focusing on sediment intervals with the highest potential for organic matter preservation. Analyses were conducted using an Elemental Analyzer Isolink system (Thermo Scientific) coupled to a Delta V Advantage isotope ratio mass spectrometer (IRMS) at the University of São Paulo. Prior to analysis, samples were freeze-dried, finely ground, and subjected to acidification to remove inorganic carbon. Decarbonation was performed through successive additions of 1 mol L⁻¹ HCl, with samples maintained in a hot water bath to enhance reaction efficiency. Following acid treatment and drying, samples were weighed into tin capsules, with sample masses adjusted according to estimated carbon content based on preliminary tests.

Biomarker analyses were performed at the University of Southern California on 53 samples spaced roughly every 30 m from representative lithologies including paleosols, fine-grained muds and silts, and sandy horizons. Samples of ∼ 60 g were extracted using accelerated solvent extraction and partitioned into hydrocarbon, polycyclic aromatic hydrocarbon (PAH), and fatty acid fractions for biomarker identification and quantification, following standard organic geochemical protocols (see Peaple et al., 2024; Karp et al., 2021).

Methane and carbon dioxide biogeochemistry. During drilling, samples were collected from the top of core sections using sterile tools and immediately stored at -4 °C until further processing. Aliquots of samples were removed for water content and total organic carbon measurements, and the remaining sample was disaggregated. For each depth, four replicates were prepared by adding 10 g of sediment in a 120 mL glass vial, sealed with butyl, and then flushed with N₂ to create an anoxic atmosphere. Incubations were carried out at 25, 35, 50, and 70 °C to simulate thermal gradients associated with sedimentary burial. During the experimental period (up to 30 d at each temperature), headspace samples were collected twice per week using gas-tight syringes (Sawakuchi et al., 2021), and concentrations of CH₄ and CO₂ were determined by gas chromatography (7890A, Agilent Technologies, Santa Clara, CA, USA) at the University of São Paulo.

Phytoliths. A total of 462 samples were taken for extraction of phytoliths and other biosilica, targeting paleosols, lacustrine sediments, and tuffs (Strömberg et al., 2018), as well as fine-grained sedimentary rock (siltstone, claystone, mudstone, fine sandstone). So far, 330 samples have been processed using standard methods (Strömberg et al., 2018), which include crushing, treatment with HCl to dissolve carbonate cements, sieving to promote deflocculation of the sediment, treatment with Schultze's solution (HNO₃ + KClO₃), and floatation with ZnBr₂-based heavy liquid, rinsing with ethanol before mounting on slides in Cargille Meltmount. The mounted sample yield was checked for biosilica recovery at 400 × using a Nikon 80i compound microscope. Phytolith morphotypes were identified using Strömberg laboratory protocols (Strömberg, 2003; Stiles et al., 2025), the literature (e.g., Dickau et al., 2013; Crifò and Strömberg, 2021; Morcote-Ríos et al., 2025), and the reference collection of phytoliths extracted from modern plants (1314 taxa) held at the Burke Museum of Natural History and Culture (UWBM), University of Washington, USA.

Ostracods. A total of 138 samples ranging from 10.55 to 913.44 m depth have been washed (dry sample weight between 20 and 140 g) and have undergone a preliminary inspection. From the lower part of the core (depth interval 768.25–913.44 m), 40 samples have been provisionally studied for their taxonomic composition. Eighteen of these samples did not contain any ostracods.

Macrofossils. Thirteen fossils of vertebrate and invertebrate animals were taken in layers distributed from 346.4 m depth to 896.2 m depth. The material was found through visual sedimentological description and has undergone a preliminary inspection for curation and taxonomy at the Federal University of Acre.

DNA geomicrobiology. Samples collected from 66 depths between 4.37 and 921.25 m were analyzed for molecular characterization of the microbial content. However, the difficulty in recovering genetic material in sufficient quantity and quality led to the need for testing multiple DNA extraction protocols. Nine distinct approaches were evaluated, including commercial kits, along with adaptations involving CTAB, phenol-chloroform, and variations in reagent volumes and soil input. Protocols described by Stirling (2003) and Kistler (2011) were also applied, aiming to overcome challenges posed by deep samples, which may contain fragmented DNA or DNA strongly adsorbed to mineral matrixes. Analytical procedures included quantification by Nanodrop and Qubit, agarose gel electrophoresis, and polymerase chain reaction (PCR) using different primer sets.

The cement bond log (CBL), acquired with the full-waveform sonic (FWS) tool, showed a good bond between the casing and the borehole wall (bond index) down to 18 m, with a median of 70 %. Below this depth, from 18 to 545 m, the bond was moderate to poor, with a median not exceeding 40 %.

The caliper log (Fig. 6) recorded recurrent washouts ranging from centimeters to meters thick. Thin intervals of washout are likely weak zones associated with the boundary between sandy and fine-grained sediment layers. Thicker washout intervals occurred below 350 m depth, where muddy sediment layers became more continuous. In general, the thickest washout intervals were observed in clay-rich sections.

In general, the natural gamma log (Fig. 6) shows a good correlation with the recorded stratigraphy, increasing in more clay-rich sections and decreasing in sandy intervals. However, this pattern was inverted in the intervals of 23.5–51 m, between 38 and 52, 70–75, and 389–391 m. The readings are significantly structured, displaying several major peaks (e.g., 72–74, 153–155, 344–347, 373, 390–391 m depth) and several lesser peaks (e.g., 202–203, 226–227, 245–246, 415, 513 m). Most of these peaks coincide with natural gamma peaks also recorded during laboratory measurements of whole cores on the MSCL (Fig. 7), which allows core-hole data comparisons. In some cases, downhole natural gamma peaks coincide with downhole magnetic susceptibility peaks (e.g., 72–74, 344–347, 373 m), with increases of two to three times, indicating a strong correlation when variations exceed 3 SI units in the magnetic susceptibility profile, although this relationship is somewhat clearer in the laboratory logging results.

The electrical logs from the GRP1000 tool showed some sections of higher permeability, indicated by a greater inflection in the single-point resistivity (SPR) and spontaneous potential (SP) curves, and a separation between the short and long resistivity curves in the intervals between 63–73, 95–110, 293–315, 319–329, 339–350, and 366–375 m. Additionally, the SPR log generally showed a response that aligned well with the lithological variations described from the cores and can be used to aid in the interpretation of sections with low core recovery or a gap.

A comparison of the fluid temperature and conductivity logs with the electrical logs shows two inflection points in the curves – one at 321 m and another at 366 m – which coincide with sections of higher permeability.

The FWS log showed good correlation with major changes in lithology, indicating a high-quality performance of the tool. In most of the profile, it was possible to identify both compressional (P) and shear (S) waves. These data will be very useful for future, more detailed analyses to determine the mechanical properties of the material and to estimate porosity, following calibration with core scan data.

The gas composition in the drilling fluid from the well is dominated by CH₄, with lower concentrations of C₂H₆, C₃H₈, and n-C₄H₁₀. OLGA measurements identified CH₄-rich zones at depths of 250–380 and 420–588 m, where C₂H₆ and C₃H₈ also show notable peaks. In contrast, i-C₄H₁₀ and n-C₄H₁₀ concentrations are lower in these intervals but increase between 600 and 700 m. CH₄ shows weak correlation with C₂H₆ (ρ = 0.34), C₃H₈ (ρ = 0.38), i-C₄H₁₀ (ρ = 0.43), and n-C₄H₁₀ (ρ = 0.43), whereas C₂H₆ and C₃H exhibit a strong correlation (ρ = 0.85). Spearman correlations (ρ) are considered significant when p < 0.05, although in this case, p > 0.05, which suggests no strong statistical significance, as reported in Martinez et al. (2025).

The stable carbon isotope analysis of eight CH₄ samples from the gas line yielded δ13C values ranging from -35 ‰ to -25 ‰. In the depth interval between 474 and 514 m, δ13C values were below -27 ‰ (Martinez et al., 2025). Additionally, the 300–314 m depth range had more negative δ13C values compared to other intervals. Additional data on downhole gas analyses are available in Martinez et al. (2025).

Pore-water values for δ18O ranged from -6.11 ‰ to -4.88 ‰, and from -38.1 ‰ to -30.5 ‰ for δ2H, with a gradient of 5.7 and an intercept (deuterium excess) of -3.1. The shallowest sample (19.4 m depth) is on the depleted end, with δ18O of -6.11 ‰ and δ2H of -37.2 ‰. Values increase with depth up to 60 m (-5.44 ‰ and -33.9 ‰), decrease to 140 m (-6.10 ‰ and -38.1 ‰), and increase again down to 630 m (-4.88 ‰ and -30.5 ‰). Intercept and deuterium excess for local rainwater values, established for Cruzeiro do Sul (10 km north of the drilling site) by Martinelli et al. (1996), are significantly different. The gradient is 8.18, similar to the Global Meteoric Water Line (GMWL) value of 8, and deuterium excess is 15.1, higher than the GMWL value of 10. Individual sample values were unfortunately not shown by the authors. The differences between local precipitation and the GMWL are caused by the evaporative cycles that rainwater undergoes during transport from the Atlantic Ocean to the studied region (Gat and Matsui, 1991; Martinelli et al., 1996). The lower gradient and deuterium excess for pore water is probably caused by water–rock interaction.

The isotopic signature of the water well samples (up to 80 m deep) overlap with the pore-water values, being closer to the more depleted end of their range: -6.04 ‰ to -5.57 ‰ for δ18O, and from -37.2 ‰ to -34.5 ‰ for δ2H. The Juruá River sample is the most enriched water we analyzed, with -2.93 ‰ for δ18O and -19.0 for δ2H. The values for shallow piezometers and the spring water overlap with part of the pore-water samples, extending to more enriched values, with δ18O ranging from -5.63 ‰ to -3.96 ‰ and δ2H ranging from -35.9 ‰ to -23.1 ‰. Since these samples were collected during a single season, the influences of seasonality cannot be evaluated, and new samples will be collected for that purpose. The drilling mud sample values fall within the pore-water range, with -5.89 ‰ for δ18O and -36.8 ‰ for δ2H, making isotopes a less effective tool to determine contamination.

Among the 306 samples that have been processed to date, 155 are sterile, and 151 have some degree of organic matter recovery. The analysis of 65 samples, with an interval of 15 m between each sample, has been completed. A total of 102 820 grains have been detected, with identifications for 39 472 of these. Sample counts range from 2 to 14 230 grains per sample, with a mean of 720 grains per sample. Palynomorphs have been detected from 54.7 to 913 m, but the palynomorph classification has only been done in 38 % of the grains. Sterile intervals include 18–57, 154–210, 406–482, 487–511, and 591–629 m. The overall palynological recovery from 631 to 913 m was higher than from 0 to 631 m. Key biostratigraphical occurrences include the Cyatheacidites annulatus FAD (first appearance datum) at 512 m, the absence of Crassoretitriletes vanraashdooveni, the LAD (last appearance datum) of Grimsdalea magnaclavata at 154 m, the LAD of Retibrevitricolporites yavarensis at 548 m, and the LAD of Echiperiporites intectatus at 788 m. The assemblage suggests that the upper 512 m is not older than 6 Ma (the hiatus and SOL-17 zones of Jaramillo et al., 2025). The interval 913–512 m could belong to zone SOL-15 and the upper SOL-14 (6 to ∼ 10 Ma), but presently there are too few samples with taxonomic classifications in this interval.

Results from six samples are included, including modern sand from the Juruá River near the well site and five sand/sandstone samples collected at 1, 178.5, 300.1, 497.4, and 863.0 m. Between 387 and 584 zircon grains were analyzed per sample to increase the chance of identifying neo-volcanic zircons, even if they constituted a minor proportion of the grains from the source areas. A seemingly robust maximum depositional age (MDA) estimate of 5.8 ± 0.21 Ma for sample 1A100Q2 at 178.5 m depth is based on 18 young grains. Remarkably, no ages younger than ∼ 6 Ma are found up-section, nor do they occur in the modern sand of the Juruá River, either reflecting the absence of volcanism since the latest Miocene in the source areas to the west along the northern Peruvian Andes or reduced deposition of latest Miocene to late Quaternary sediments in this part of the Acre Basin. Down-section, MDA estimates increase to 7.8 ± 0.5 Ma (300.1 m), 8.6 ± 0.2 Ma (497.4 m), and 11.8 ± 0.4 Ma (863 m). Thus, our current MDA results suggest that strata at the bottom of the well (923 m) were likely deposited around 12 Ma or somewhat younger. Detrital zircon age populations are multi-modal and remarkably similar in all samples, with a dominant Permo-Triassic age population. A control sample collected in a modern sand bar of the Juruá River (n = 437), close to the drilling location, shows similar age distributions, albeit with the appearance of a Jurassic population, an increase in the Cenozoic age peak, and a reduction in the Permo-Triassic population (Fig. 9). Our age constraints allow us to unambiguously document a dominant Andean contribution to the sedimentary budget accumulated in the Acre Basin in the recovered sequence, although the data do not entirely preclude the possibility of the recycling of Andean sediments that were previously deposited upstream in the Acre region.

Preliminary results indicate that quartz natural OSL signals are saturated for two samples tested: one at 1.3 m and the other at 10 m depth. Minimum equivalent doses are 135 ± 8 Gy (n = 9) and 180 ± 13 Gy (n = 5), based on the double of the characteristic dose (2D₀). Hence, quartz OSL dating provides only minimum sediment deposition ages. Given the dose rates of 1.51 ± 0.09 and 1.91 ± 0.12 Gy ka⁻¹ for quartz, the samples at 1.3 and 10 m depth would correspond to minimum ages of 89 and 94 ka, respectively. Feldspar natural pIRIR₂₉₀ signals were also in saturation for samples at 4 and 21 m depth, indicating minimum equivalent doses of approximately 600 Gy. Average values of 2D₀ for the pIRIR₂₉₀ was 616 ± 14 Gy (n = 5) for the 4 m depth sample and 630 ± 36 Gy (n = 5) for the 21 m depth sample. The residual doses of up to 100 Gy may occur in pIRIR₂₉₀ signals from fluvial sediments in the Amazon, and, thus, true equivalent doses may be approximately 500 Gy here. Considering the 2D₀ of 630 Gy and dose rates of 3.19 ± 0.18 Gy ka⁻¹ for feldspar, the sample at 21 m depth would correspond to a minimum age of 198 ka. Thus, both quartz OSL and feldspar pIRIR₂₉₀ dating suggest that sediments in the upper portion of the core were deposited beyond ∼ 200 ka.

Quartz OSL sensitivity (%BOSL_1 s) in polymineral aliquots is relatively low, ranging from 3 % to 7 % in the interval from 15 to 923 m depth. The 580–640 and 750–923 m depth intervals show sediment layers with %BOSL_1 s reaching 6 %–7 %. Brighter quartz grains are observed only in the upper 10–15 m depth, with %BOSL_1 s in the 15 %–30 % range. The IRSL_1 s / OSL_1 s ratio indicates sands rich in feldspar, except for the upper 15 m, which has a low feldspar content. In summary, preliminary luminescence analysis indicates the dominance of immature feldspar-rich sands supplied from sources with high denudation rates, similar to Andean sands transported by the Solimões and Madeira rivers (Sawakuchi et al., 2018). The upper 10–15 m has higher maturity sands, with quartz grains supplied by lower denudation rate sources, possibly from recycled Andean sediments or a mixture between Andean and cratonic sources.

Heavy mineral samples from the Acre drill core contain a variety of minerals, which include epidote, zircon, rutile, tourmaline, garnet, kyanite, andalusite, sillimanite, enstatite, hypersthene, hornblende, augite, and diopside. The initial results of quantification of the heavy minerals assemblage allow for a preliminary picture of the heavy mineral composition in the lower half of the Acre drill core. Clinopyroxene concentration (mostly augite and diopside) ranges from 7 % to 24 %, whereas orthopyroxene (hypersthene and enstatite) concentrations are comparatively higher, ranging from 2 % to 30 %, with a majority of samples exceeding 20 %. Both populations show no clear variation in the concentration along the core extent. Hornblende concentration shows significant variation, ranging from below 5 % up to 60 %, with a tendency of enrichment toward the major erosional surface at the 536 m depth. Aluminosilicates (mostly andalusite and staurolite, with minor kyanite) often sum up to 5 % to 10 % of the heavy minerals, with a few exceptions surpassing 12 %, trending below 5 % toward the 536 m erosional surface. Garnet grains, similarly, have abundances often in the 5 % to 10 % range from the base, trending under 5 % toward the 536 m depth. Ultra-stable minerals (zircon, rutile, and tourmaline) account typically for values around 20 % of the samples, with a few exceptions slightly surpassing 30 %, with a gradual impoverishment (down to 5 %) toward the 536 m erosional surface.

Although the heavy mineral results are still preliminary in nature, they show some gross trends of heavy mineral compositional change along the lower half of the Acre drill core. The relatively abundant assemblage rich in augite, hypersthene, and hornblende resembles the heavy mineral assemblages found in the modern Amazon River channels (Nascimento et al., 2015), suggesting that most of the provenance sources are from basic igneous rocks from the Andean Range. The less frequent contribution from aluminosilicates and ultra-stable minerals suggests that low- to medium-grade metamorphic rocks, and even plutonic rocks, may play a minor role in the sediment sourcing. These minor sources have a progressively lower presence toward the erosional surface at the 536 m depth, indicating a prevalent and growing component of Andean sources from the bottom of the Acre drill core up to the middle of the drilled sequence.

ICP-MS data demonstrate that the cosmogenic samples were successfully purified, and quartz grains were isolated. Despite significant material loss during physical separations and acid treatments, enough material remained for dissolution and chemical fractionation (25 to 46 g). Due to the naturally low Be content in the sediments, a known amount of ¹⁰Be (approximately 0.23 mg) was added to each sample. After undergoing the chemical separation steps of hydroxide co-precipitation (to remove Mg, Mn, K, and Ti) and isotopic fractionation columns for Fe, Be, and Al, high recovery rates of Be (85 %–92 %) and Al (89 %–99 %) fractions were recorded relative to the total sample aliquot. The results indicate that the samples from the first 75 m, even with relatively small masses for in situ cosmogenic nuclide analysis in basins with low isotopic production rates (such as the Acre Basin), are promising for the use of the ¹⁰Be and ²⁶Al pair in analyses.

Magnetic susceptibility remains positive throughout the entire TADP-1A core (Fig. 10). Furthermore, magnetic susceptibility measurements taken along core sections and on oriented samples exhibit good agreement. The magnetic susceptibility of oriented samples ranges from 5.60 × 10⁻⁸ to 7.60 × 10⁻⁷ m³ kg⁻¹, with an average value of 1.50 × 10⁻⁷ m³ kg⁻¹. The highest MS values are observed in the lower portion of the core, at a depth of approximately 750–800 m. MS values are lower toward the top of the core, reaching a minimum at a depth of 1.7 m. The high positive MS values suggest a main contribution of paramagnetic and/or ferrimagnetic minerals. Based on the χFD% values, there is a predominance of particles with values lower than 4 % at the base of the core, indicating a prevalence of larger grains, characterized as MD (multi-domain) or PSD (pseudo-single domain) particles. Above 350 m depth and toward the top section, the χFD% values increase to above 5 %, suggesting a primary contribution from SP (superparamagnetic) grains. Some significant variations, or peaks, may indicate changes in sedimentation rates or the presence of different magnetic minerals within the core. Further magnetic analyses will be conducted to determine the magnetic carriers and their specific characteristics.

εNd values vary between -11.1 and -9.9 (average -10.5 ± 0.7 (2 SD)). εNd values generally decrease from the bottom to the top of the record, but this trend is not statistically significant with the current analytical results. ⁸⁷Sr / ⁸⁶Sr values vary between 0.7187 and 0.7312 (average 0.7232 ± 0.0062 (2 SD)). ⁸⁷Sr / ⁸⁶Sr values are relatively low from the bottom of the record until ∼ 525 m depth, increase until ∼ 300 m depth, decrease again until ∼ 45 m depth, and increase, reaching the maximum values in the uppermost two samples of the record.

In general, εNd and ⁸⁷Sr / ⁸⁶Sr values form a narrow cloud of points within the typical values reported for the eastern tropical Andes, the Altiplano, and the tropical Subandean foreland (Pinto, 2003). As a result, they coincide with the expected values for a mixture of suspension sediments from the Solimões and Madeira rivers (Allègre et al., 1996; Viers et al., 2008; Bouchez et al., 2011; Höppner et al., 2018), the two main Andean tributaries of the Amazon River, and are in agreement with suspension sediments found at the mouth of the Amazon River, as well as offshore from the mouth (Zhang et al., 2015; Höppner et al., 2018).

The outcropping layers with ferruginous clasts from four sites consist mainly of a hematite phase with residual quartz grains, while the Fe-lateritic duricrust sample is composed of a hematite layer rich in kaolinite and a pure goethite layer. Each mineralogical phase was dated, and preliminary (U–Th) / He data were obtained only from the hematite in the iron-enriched samples and the goethite layer in the Fe-lateritic duricrust. Notably, all aliquots yielded systematic Quaternary ages, with values ranging from approximately 0.4 ± 0.2 to 1.0 ± 0.5 Ma, although with large uncertainties due to low helium content. Despite the significant errors in these preliminary data, all ages fall within the Quaternary period, and no age difference was detected between the stonelines and the Fe-lateritic duricrust samples. However, the chemistry of these samples differs markedly: the stonelines (hematite) exhibit U concentrations of 1 to 6 ppm and Th concentrations of 5 to 23 ppm, whereas the goethite extracted from the Fe-lateritic duricrust shows U concentrations similar to those of hematite (3–8 ppm) but significantly lower Th concentrations (1–2 ppm). Additional data are currently being acquired to refine and improve the accuracy of the (U–Th) / He ages, but we can now conclude that the host sedimentary formation is older than 1 Ma. Where Fe-clasts from the TADP-1A core were examined and found to contain porous mixed Fe-Mn oxide phases, the purest samples were prepared for ongoing (U–Th) / He dating.

Among the many major elemental ratios, we report ln⁡(Al / Si) and ln⁡(Fe / K), because of their strengths and applicability to track sources of sediments transported by Amazon fluvial systems (Bouchez et al., 2011; Govin et al., 2012; Zhang et al., 2017; Grigolato et al., 2025). Minimum and maximum ln⁡(Al / Si) values are -2.72 and -1.03, respectively, whereas the average value is -1.43. The ln⁡(Al / Si) values are relatively stable throughout the analyzed portion of the record, with three notable excursions toward lower values: (i) between ∼ 111 and ∼ 99 m below the surface; (ii) between ∼ 77 and ∼ 63 m depth; and (iii) between ∼ 55 and ∼ 38 m depth. Minimum and maximum ln⁡(Fe / K) values are -0.70 and 1.49, respectively, while the average value is 0.56. The behavior of the ln⁡(Fe / K) values is similar to that of the ln⁡(Al / Si), but ln⁡(Fe / K) values show two additional excursions toward lower values, namely between ∼ 228 and ∼ 214 m depth and between ∼ 30 and 15 m depth.

While ln⁡(Al / Si) can be considered a proxy for grain size (the smaller the grain size, the higher the ratio) for sediments from the Amazon rivers (Bouchez et al., 2011; Sun et al., 2017), ln⁡(Fe / K) has been used as a proxy for distinguishing Andean versus lowland sources of sediments (the more Andean sediments, the lower the ratio) (Bertassoli et al., 2019; Grigolato et al., 2025), as well as changes in the strength of chemical weathering of sediment sources (the stronger the chemical weathering, the higher the ratio) (Zabel et al., 2001; Govin et al., 2012). Because the Andes seems to be the primary source of sediments (see results from various proxies), ln⁡(Fe / K) may be primarily controlled by chemical weathering. The three excursions toward lower ln⁡(Al / Si) and ln⁡(Fe / K) values suggest the occurrence of coarser less-weathered sediments (Bouchez et al., 2011; Grigolato et al., 2025). Interestingly, the average ln⁡(Fe / K) value (0.56) of our record is similar to the average value of modern suspended sediments of the Solimões (1.02) and Madeira (0.71) rivers (Grigolato et al., 2025). Completing the major elemental analyses for the whole drilled section, as well as performing other types of analyses (e.g., grain size), is necessary to support in-depth interpretations.

XRD analysis of all samples yielded average contents of 45.7 % ± 27.9 (2σ) for quartz, 29.5 ± 29.3 for clay minerals plus mica, 20.5 ± 14.2 for feldspar, 3.9 ± 12.4 for carbonates, and 0.4 ± 1.3 for other minerals. The high standard deviation values reflect the compositional variability between lithotypes, mainly represented by sandstones and mudstones. Sandstones average 55.1 ± 13.3 for quartz, followed by feldspar at 22.2 ± 14.7, clay minerals plus mica at 20.5 ± 15.6, carbonates at 1.8 ± 4.8, and other phases at 0.4 ± 1.6. The high feldspar content of the sandstones indicates low mineralogical maturity, consistent with the occurrence of arkosic composition, whereas the elevated clay mineral proportion may be related to in situ feldspar alteration. Mudstones average 42.4 ± 24.6 for clay minerals plus mica, 32.3 ± 19.9 for quartz, 18.1 ± 12.0 for feldspar, 6.8 ± 16.7 for carbonates, and 0.4 ± 0.5 for other minor phases. As expected, these fine-grained siliciclastic rocks have a higher clay mineral content (Tucker and Jones, 2023). The relatively high carbonate content may be linked to early diagenetic processes within the sediment.

TOC concentrations ranged from below the analytical detection limit to a maximum of 15.58 % (med = 0.06 %), with the highest values observed between approximately 500 and 720 m depth. The generally low TOC values throughout much of the record suggest extensive post-depositional degradation under oxic conditions. Although clay-rich facies are typically more favorable for organic matter preservation due to their low permeability and protective matrix, no clear correlation was identified between TOC content and grain size in the analyzed sample set. This suggests that rapid sedimentation events, capable of rapidly burying organic material and isolating it from oxidative degradation, may have played a key role in enhancing TOC preservation in portions of the record. The δ13C of samples with TOC contents exceeding 0.15 % ranged from -26.28 ‰ to -24.66 ‰, consistent with a dominant contribution from C₃ terrestrial vegetation in these intervals.

Concentrations of sedimentary hydrocarbons are high in two intervals of the core: ∼ 150–250 m and below 500 m. Outside these intervals, sediments have low hydrocarbon yields that are more degraded and/or mature, and less amenable to environmental reconstruction. Sediments contain n-alkanes, n-alkanoic acids, PAHs, and macrofossils that allow aspects of plant producers and depositional environments to be detected. No substantial heating and alteration occur in situ; however, low temperature, oxic degradation, and diagenesis likely explain the low abundances of biomarkers in the core in general. Low concentrations of n-alkanes (< 1 µg gdw⁻¹) combined with maturity/degradation in the majority of samples precludes compound-specific C or H isotope analysis. δ13C measurements on higher concentration n-alkanoic acids (< 5 µg gdw⁻¹) yielded values ranging from -27.2 ‰ to -36.6 ‰, also consistent with a C₃ terrestrial vegetation signal. PAHs are detectable and commonly include retene, often used to denote the presence of gymnosperms, which is surprising as gymnosperms are rarely detected in the pollen assemblages; thus, other possible producers or diagenetic pathways appear likely.

Preliminary results from the incubation experiments of sediment samples collected at 140.82 and 502.42 m depth show that, after 22 d of incubation at 25 °C, no detectable methane (CH₄) production occurred. In contrast, both samples exhibited a progressive increase in CO₂ concentrations that could be related to microbial activity or chemical weathering of inorganic carbon in the samples. The accumulation of CO₂ without concomitant CH₄ production suggests that processes other than methanogenesis are currently dominant, but it is still early to draw any conclusions as similar incubations using old subsurface sediment had a lag-phase longer than 30 d before CH₄ production started (Harris et al., 2008). In addition,  substrate limitations, or competitive inhibition by alternative microbial processes, such as sulfate or iron reduction, could also limit or delay the production. These results highlight the importance of extending the incubation time beyond the initial 22 d to determine whether methane production will eventually occur once favorable redox conditions are established or labile substrates are consumed. Isotopic analysis of ¹³C in CO₂ and eventually CH₄ at the end of the incubation period will help us to understand the pathways of production of these gases. Incubation experiments will help to determine if the methane detected regularly during drilling is partially derived from an active microbial gas system, a product of an ancient inactive microbial gas system, or migrated from a deep burial thermogenic gas system.

To date, 1852 palynomorph species have been identified. The abundance of grass pollen increases to 12 % on average in 131 to 154 m, whereas there is a short spike of abundant Podocarpus at around 244 m, which suggests colder/drier conditions than modern. There is reworking of Cretaceous material in the 486 to 585 m interval. Many of the dominant floristic elements of the Pebas system (Jaramillo et al., 2025) are rare in the core, suggesting that the flora of the core belongs to a post-Pebas ecosystem that has rarely been studied as its sediments are rarely preserved. Most of the floral diversity is dominated by angiosperms, with no evidence of marine or brackish conditions. There are samples with high levels of diversity (up to 183 taxa in a count of 745), many of them being rare (one or two individuals), similar to modern rainforests.

The 330 processed samples, which capture all but the top 140 m of the core, have been checked for phytolith recovery. The vast majority of these (300, or 91 %) did not yield any biogenic silica, and most also did not contain volcanic ash and secondarily precipitated silica, two types of non-biogenic silica with specific gravities that overlap with that of biosilica. So far, only 29 samples (8.8 %) featured rare phytoliths or diatoms, sponge spicules, and chrysophyte cysts that were well preserved. Among the phytolith morphotypes present, we identified potential palm phytoliths (SPHEROID ECHINATE) and an armed trichome (diagnostic of certain dicotyledonous angiosperms; Piperno, 2006), as well as less diagnostic forms (ELONGATE ENTIRE, ELONGATE DENTATE, and BLOCKY), all of which were exceedingly rare (one or two grains per slide). These marginally productive samples derive from lithologies ranging from claystone to sandstone, pointing to no clear pattern of preferential preservation linked to lithology. Because of the rarity of biosilica particles, we cannot rule out contamination during sample collection or processing. The overall lack of biosilica and other light silica (opal-A and similar) suggests that the chemical environment in the Acre core was not conducive to silica preservation in general, for example, due to high pH or abundant organic material, both of which have shown to accelerate silica dissolution (e.g., Song et al., 2016).

In the upper portion of the drill core record (0–513 m), the ostracod record is extremely poor, likely due to the depositional environment, which primarily is represented by paleosols. An interval in the lower sections of the core (789.02–793.30 m) contains a small number of ostracods, with at least three species of the ostracod genus Cyprideis (Fig. 11). Although very preliminary, these taxa are similar to those that are characteristic of the Pebas fauna (Gross et al., 2014; Gross and Piller, 2020).

Macrofossils of plants, crustaceans, and vertebrates were found in several stratigraphic layers during the description and sampling of the Acre drill core. Preliminary identifications suggest that the fragments are reworked material derived primarily from sandy-conglomeratic layers and are associated with plant debris, coal associated with pyrite, rounded to sub-angular carbonate and cemented sandstone clasts, and mudclasts. These layers correspond to facies association FA1, and represent sharp erosional surfaces and/or co-sets of conglomerate and sandstone stacking. The only sample that differs from this relationship is 717.69 m, derived from mottled mudstone with peds, and rare and scarce iron hydroxide concretions. Preliminary identifications include crocodile teeth and a possible mammal bone, which ultimately could help to constrain sedimentation ages for the cores.

Fossils found in the following core sections are preliminarily identified as mammal rib and fish scales (882 m), an Actinopterygii fish tooth (497.95 m), fossil wood and a Potamotrygonidade stingray tooth (894.99 m), a possible mammal bone and coprolites (839.37 m), an Erythrinidae fish tooth (610.25 m), fish bone (842.09 m), a Eusuchia crocodylomorpha tooth (731.32 and 557.07 m), and a Tricholdactylidae crab pincer (717.69 m).

DNA extractions were consistently unsatisfactory: Qubit readings ranged from 0.08 to 0.2 ng µm⁻¹, no bands were observed on agarose gels, and all PCR attempts yielded negative results. Purification strategies, such as acetate or ethanol precipitation, QIAquick PCR purification kit, and magnetic beads also failed to significantly improve outcomes. These findings reflect challenges reported in other deep drilling projects, such the Collisional Orogeny in the Scandinavian Caledonides (COSC) project in Sweden. Westmeijer et al. (2024) reported similar difficulties when attempting to characterize microbial communities in deep rock samples. Despite applying six optimized extraction protocols and rigorous contamination control using fluorescent beads, the DNA extracted from core samples remained below detection limits, indicating extremely low biomass. Additionally, the Swedish study highlighted that, even after removing potential contaminants associated with drilling fluid, most sequences were affiliated with microorganisms known to be common reagent contaminants. The detection of native deep biosphere taxa, such as Candidatus Desulforudis audaxviator, occurred at levels below 0.1 % of total sequences, thus hindering any ecological interpretation. Given these challenges, the use of ancient DNA (aDNA) recovery strategies is suggested as a possible approach for future studies, involving specific reagents and techniques developed for low-biomass environments.