# Cooling and Exhumation History of the Paris Basin Southeastern Margin Revealed by Δ47/U-Pb Carbonate Thermochronology

Marta Gasparrini, Xavier Mangenot, Magali Bonifacie, Pierre Deschamps, Andrea Ceriani

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Marta Gasparrini, Xavier Mangenot, Magali Bonifacie, Pierre Deschamps, Andrea Ceriani. Cooling and Exhumation History of the Paris Basin Southeastern Margin Revealed by Δ47/U-Pb Carbonate Thermochronology. Terra Nova, 2025, 37 (6), pp.421-430. 10.1111/ter.70004. hal-05455616

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# Cooling and Exhumation History of the Paris Basin Southeastern Margin Revealed by Δ₄₇/U-Pb Carbonate Thermochronology

Marta Gasparrini<fnref n="1" /> ID | Xavier Mangenot²,³,⁴ ID | Magali Bonifacie⁵ ID | Pierre Deschamps⁴ ID | Andrea Ceriani⁶ ID

**Correspondence:** Marta Gasparrini (marta.gasparrini@unimi.it)

**Received:** 1 February 2025 | **Revised:** 25 June 2025 | **Accepted:** 16 July 2025

**Funding:** This work was supported by IFP Energies nouvelles, Khalifa University of Science, Technology and Research, Award No. CIRA-2021-048. Ministero dell'Università e della Ricerca, Dipartimenti di Eccellenza 2023-2027.

**Keywords:** clumped isotopes (Δ₄₇) | diagenetic carbonates | exhumation rates | LA-ICPMS U-Pb dating | meteoric recharge

## ABSTRACT

This study applies Δ₄₇/U-Pb thermochronology to the Middle Jurassic carbonates exposed in the southeastern margin of the Paris Basin. By integrating clumped isotope analyses and U-Pb dating of diagenetic carbonates, we reconstruct the thermal and exhumation history of the sedimentary succession. The results revealed the occurrence of four diagenetic phases that precipitated from Early Paleogene to Quaternary, reflecting episodic meteoric fluid recharges and gradual cooling during tectonic uplift. Our findings indicate two major uplift periods, linked to the Pyrenean (Palaeocene to Mid-Eocene) and Alpine (Early Miocene to Quaternary) compressional phases, with exhumation rates of 37 m/Ma and 25 m/Ma, respectively. Total erosion is estimated at ~1000 ± 200 m and is consistent with regional apatite fission-track data. These findings establish Δ₄₇/U-Pb carbonate thermochronology as a robust tool for studying uplift dynamics and cooling/exhumation rates in sedimentary basins and mountain ranges and pave the way for applications worldwide.

## 1 | Introduction

Low-temperature thermochronology of sedimentary successions provides insights for constraining the thermal history of sedimentary basins. It may enable estimation of hydrocarbon generation timing, determine the onset and progression of tectonic inversion, and quantify basin exhumation rates. Historically, these reconstructions have relied on thermo-chronometers such as fission-tracks and (U-Th)/He analyses (e.g., Peyton and Carrapa 2013; Malusà and Fitzgerald 2019) that are, however, not suitable for successions dominated by carbonate rocks.

Recent advances in carbonate isotope geochemistry and mass spectrometry have now made it possible to quantify the timing of heating/cooling events in carbonate-bearing rocks. This is achieved through the application of Δ₄₇/U-Pb thermochronology on diagenetic carbonates (sensu Mangenot, Gasparrini, Gerdes et al. 2018), an innovative approach that combines clumped isotope (Δ₄₇) analyses with LA-ICP-MS U-Pb dating. This approach has been applied in various studies to address a range of geological questions. For instance, it has been used to reconstruct the burial history of sedimentary successions (Lawson et al. 2018), reveal early dolomite recrystallisation

<footnote n="1">¹Earth Sciences Department, University of Milan, Milan, Italy | ²H-Expertise Services, Pomps, France | ³IFP Energies nouvelles, Rueil-Malmaison, France | ⁴Aix Marseille Univ., CNRS, IRD, INRAE, CEREGE, Aix-en-Provence, France | ⁵Université Paris Cité, Institut de Physique du Globe de Paris, CNRS, Paris, France | ⁶Earth Sciences Department, Khalifa University of Science and Technology, Abu Dhabi, UAE</footnote>

<footnote>[Corrections added on 8 August 2025, after first online publication: Minor textual alterations have been made to this version of the article at the request of the Corresponding Author.]</footnote>

<footnote>This is an open access article under the terms of the Creative Commons Attribution License, which permits use, distribution and reproduction in any medium, provided the original work is properly cited.</footnote>

<footnote>© 2025 The Author(s). Terra Nova published by John Wiley & Sons Ltd.</footnote>
(Gasparrini et al. 2023), constrain deformation conditions in brittle rocks (Hoareau et al. 2021; Blaise et al. 2022), assess hydrothermal fluid circulation in sedimentary systems (Brigaud et al. 2020), and achieve quantitative paragenesis in carbonate-bearing rocks (Pan et al. 2021; Li et al. 2024). However, the potential of this approach to reconstruct uplift dynamics and corresponding cooling/exhumation rates remains far less explored.

Building on these advances, we applied here the $\Delta_{47}/U-Pb$ thermochronology approach to investigate the exhumation history of the Middle Jurassic carbonate succession from the southeastern margin of the Paris Basin that presently crops out in the Burgundy region (Floquet et al. 1989; Gaumet et al. 1996). The chosen stratigraphic interval stands out for the exceptional exposure in quarries, the occurrence of multiple generations of macroscopic diagenetic carbonates, and the mild thermal history (Uriarte 1997; Beaudoin et al. 2019; Vergara Sassarini et al. 2023) that allowed preservation of original carbonate $\Delta_{47}$ compositions (Mangenot et al. 2017; Mangenot, Gasparini, Rouchon, and Bonifacie 2018; Vergara Sassarini et al. 2024). It represents an ideal natural laboratory for testing and advancing the $\Delta_{47}/U-Pb$ thermochronology approach in the very low-temperature (50°C–100°C) domain.

## 2 | Geological Setting

The Paris Basin is a well-studied Meso-Cenozoic intracontinental basin (e.g., Brunet and Le Pichon 1982; Pomerol 1989; Perrodon and Zabek 1990) bounded by ancient Hercynian masses: the Ardennes to the NE, the Armorican Massif to the W, the Vosges to the E and the Massif Central to the S (Figure 1). The basin depocentre is filled with up to 3000m of Permian to Quaternary deposits, mainly of Meso-Cenozoic age, resting on deformed Palaeozoic basement (Delmas et al. 2002; Guillocheau et al. 2000). At the surface, concentric outcrops of Meso-Cenozoic deposits (Figure 1) reveal exhumation and erosion, driven by Late Cretaceous and Tertiary deformation linked to Africa-Europe convergence (Ziegler 1988), that were significantly more pronounced along the basin margins compared to the depocentre. The Pyrenean and Alpine compressional phases reactivated ancient structures and were separated by an Oligocene extensional event in the southeastern part of the basin (Perrodon and Zabek 1990; Lacombe et al. 1990; Guillocheau et al. 2000).

In the Burgundy region, in the southeastern Paris Basin, Middle Jurassic (Bathonian-Callovian; 168–161 Ma) carbonate platform deposits are well exposed and today exploited as stone flooring material (Floquet et al. 1989; Gaumet et al. 1996; Makhloufi

<figure><img src="image_3.png" /></figure>

**FIGURE 1** | (A) Geological map of the Paris Basin (from Delmas et al. 2002), showing the study area. Green and yellow dots indicate the studied quarries (named Buffon and Etrochey) while the red dot (Parly) indicates the location of a well which thermal history is presented in Figure 5. (B) NW-SE geological cross-section of the Paris Basin (from Delmas et al. 2002), illustrating the Middle Jurassic stratigraphic interval both in outcrops and in the subsurface. Note that only the faults affecting the Palaeozoic and Triassic succession are illustrated. (C) View of the Buffon quarry, with the sampled *Calcaire de Comblanchien* and *Dalle Nacrée* formations separated by a hardground surface (dashed line). (D) Lithostratigraphic chart of the of the Middle Jurassic carbonates at the Buffon quarry. (E, F) Hand specimen photograph and corresponding thin-section scan of the sample BUF4a. (G, H) Hand specimen photograph and corresponding thin-section scan of the sample BUF6. [Colour figure can be viewed at wileyonlinelibrary.com]
et al. 2013). These deposits include: (1) the *Oolithe Blanche* Formation (Bathonian), consisting of grainstone (rarely packstone) from a high-energy shoal environment, (2) the *Calcaire de Comblanchien* Formation (Bathonian) composed mainly of wackestone to packstone from a protected lagoon environment, and (3) the *Dalle Nacrée* Formation (Callovian), comprising oolitic and bioclastic grainstone to packstone deposited in shoal to open platform environments.

This stratigraphic succession is time-equivalent to the main geothermal and hydrocarbon subsurface reservoirs exploited in the basin depocentre (Delmas et al. 2002; Jaudin et al. 2009), where diagenetic evolution and cementation history are well characterised (Mangenot, Gasparrini, Rouchon, and Bonifacie 2018; Mangenot, Gasparrini, Gerdes, et al. 2018, and references therein). In contrast, the diagenesis of this succession exposed in the southeastern basin margin remains poorly documented.

### 3 | Sampling and Methods

Middle Jurassic carbonate samples were collected from two quarries located between the villages of Montbard and Châtillon-sur-Seine (Figure 1), and specifically from the Bathonian *Calcaire de Comblanchien* Formation (nine samples) and the Callovian *Dalle Nacrée* Formation (two samples). Sampling targeted voluminous diagenetic carbonates visible with naked eye. Petrographic analysis was performed using optical microscopy in plane-polarised light and cold-cathodoluminescence (CL) microscopy on 60 µm-thick polished thin-sections. The CL analyses were conducted using an 8200 Mk5 CITL apparatus under vacuum (<0.1 mbar) with operating conditions of 10 kV and 250 µA. Petrographic observations allowed distinguishing different carbonate diagenetic phases and guided sample selection for subsequent geochemical analyses.

Comprehensive review of clumped isotope ($\Delta_{47}$) analyses and LA-ICP-MS U-Pb dating of carbonates can be found respectively in Roberts et al. (2020) and Huntington and Petersen (2023), and references therein. These two methodologies were here jointly applied to the different diagenetic carbonates identified.

All thin-sections were considered for U-Pb dating via LA-ICP-MS at the *Centre de Recherche et d'Enseignement des Géosciences de l'Environnement* (CEREGE). The samples were first screened to identify zones with an adequate signal of uranium and lead, and large variability in the U/Pb ratio, following the recommendations of Horstwood et al. (2016).

Eleven carbonate powders were extracted from the same rock slabs used to prepare thin-sections, using a manual drill. The powders (~5–8 mg per replicate) were analysed for $\Delta_{47}$ compositions at *Institut de Physique du Globe de Paris* (IPGP) following published protocols (Mangenot et al. (2017); Mangenot, Gasparrini, Gerdes, et al. (2018)) and converted to temperatures ($T\Delta_{47}$) using the calibration of Bonifacie et al. (2017). The oxygen isotope composition of carbonate parent water ($\delta^{18}O_w$) was calculated from $T\Delta_{47}$ and $\delta^{18}O$ of carbonates, using the fractionation equation from O'Neil et al. (1969) for calcites. Carbonate $\delta^{13}C$ and $\delta^{18}O$ values

are expressed in $\textperthousand$ relative to VPDB. Parent fluid $\delta^{18}O_w$ values are expressed in $\textperthousand$ relative to VSMOW.

Suitable carbonate phases were analysed for $\Delta_{47}$ thermometry and U-Pb dating, providing 10 paired temperature–time constraints. Methodology and data processing are provided in Supporting Information S2 and S3.

### 4 | Results

Thin-section petrography identified four different carbonate diagenetic phases (Table 1), including three calcite cements (Cal1, Cal2 and Cal3) and one dedolomite (Ded). All three calcites are non-ferroan and consist of equant blocky crystals (200–600 µm), locally exhibiting a drusy arrangement. The calcite cements primarily precipitated within fractures and moldic to vuggy pores, the latter formed by the dissolution of corals and bivalves. They were distinguished petrographically based on their different CL responses (Figure 2): Cal1 (the most common and abundant phase), mostly uniform (locally zoned) and very dull red; Cal2, uniform and very bright orange; Cal3, uniform and dull red.

The dedolomite phase (Ded; Figure 2) corresponds to a saddle dolomite cement precipitated in coral moulds prior to Cal1 that was then fully replaced by calcite. The calcite crystals still retain the scimitar-like habitus of saddle dolomite, exhibit a brownish colour due to precipitation of iron oxides, and display a non-luminescent to bright orange response under CL.

Details of the U-Pb isotopic analyses are provided in Table 1, and Supporting Information S2 (including Table S2a,b), with individual U-Pb isochrons and corresponding ages illustrated in Figure 3. The measured U and Pb isotopic ratios yield Tera-Wasserburg linear regressions (isochrons) that indicate ages from 65.6 ± 5.6 Ma to 1.9 ± 3.5 Ma, with MSWD between 1.2 and 14. Initial $^{207}\text{Pb}/^{206}\text{Pb}$ ratios show noticeable variations, ranging between 0.87 and 0.51. Notably, all U-Pb ages are systematically younger than the host-rock stratigraphic age (168–161 Ma) and point towards different Cenozoic to Quaternary diagenetic events. The U-Pb ages for the four carbonate phases are as follows: Cal1 ($n=7$) from 65.6 ± 5.6 Ma to 48.9 ± 7.3 Ma, with a mean of 56.1 Ma; Cal2 ($n=1$) is 41.6 ± 1.4 Ma; Cal3 ($n=1$) is 19.0 ± 4.1 Ma; and Ded ($n=1$) is 1.9 ± 3.5 Ma.

Details of the stable isotope geochemical analyses are provided in Table 1, Figure 4, and Supporting Information S3 (including Table S3a,b). The $\delta^{18}\text{O}$, $\delta^{13}\text{C}$, and $\Delta_{47}$ compositions of the four carbonate diagenetic phases are as follows. Cal1 ($n=7$) samples have $\delta^{18}\text{O}$ values between −13.5‰ and −10.1‰ (mean: −11.5‰) and $\delta^{13}\text{C}$ values from 0.3‰ to 2.5‰ (mean: 1.6‰). They precipitated at $\Delta_{47}$ temperatures of 37°C–49°C from fluids with $\delta^{18}\text{O}_w$ of −7‰ to −5‰. Cal2 ($n=2$) samples exhibit $\delta^{18}\text{O}$ values of −7.4‰ and −7.5‰ (mean: −7.5‰) and $\delta^{13}\text{C}$ values of 1.9‰ and 2.0‰ (mean: 2.0‰). They precipitated at temperatures of 23°C–32°C from fluids with $\delta^{18}\text{O}_w$ of −5‰ to −3‰. Cal3 ($n=1$) sample has $\delta^{18}\text{O}$ and $\delta^{13}\text{C}$ values of −8.0‰ and 1.7‰, respectively, and precipitated at ~22°C from a fluid with $\delta^{18}\text{O}_w$ of −6‰. The Ded ($n=1$) sample has $\delta^{18}\text{O}$ and $\delta^{13}\text{C}$ values of −7.2‰ and −2.2‰, respectively, and formed at ~9°C from a fluid with $\delta^{18}\text{O}_w$ of −8‰.
<table><caption>TABLE 1 | Details on the carbonate samples analysed and corresponding stable and radiogenic isotope data.</caption><thead><tr><th>Sample ID</th><th>Quarry</th><th>Occurrence</th><th>Carbonate phase</th><th>CL response</th><th>δ<sup>18</sup>O %<sub>o</sub> (VPDB)</th><th>δ<sup>13</sup>C %<sub>o</sub> (VPDB)</th><th>Δ<sub>47</sub> %<sub>o</sub> (CDES)<sup>a</sup></th><th>n</th><th>TΔ<sub>47</sub> (°C)<sup>b</sup></th><th>δ<sup>18</sup>O<sub>w</sub> %<sub>o</sub> (VSMOW)<sup>c</sup></th><th>U-Pb Age (Ma)</th><th><sup>207</sup>Pb/<sup>206</sup>Pb<sup>d</sup></th></tr></thead><tbody><tr><td>BUFcorail2</td><td>Buffon</td><td>Moldic pore</td><td>Cal1</td><td>Zoned, bright to very dull red</td><td>-11.1±0.1</td><td>1.6±0.1</td><td>0.638±0.002</td><td>2</td><td>38±2</td><td>-6</td><td>65.6±5.6</td><td>0.83</td></tr><tr><td>BUF5</td><td>Buffon</td><td>Moldic pore</td><td>Cal1</td><td>Uniform, very dull red</td><td>-11.4±0.0</td><td>1.8±0.0</td><td>0.621±0.028</td><td>2</td><td>45±13</td><td>-5</td><td>60.4±8.4</td><td>0.55</td></tr><tr><td>BUF4a</td><td>Buffon</td><td>Moldic pore</td><td>Cal1</td><td>Uniform, very dull red</td><td>-13.5±0.4</td><td>1.8±0.4</td><td>0.622±0.032</td><td>3</td><td>44±10</td><td>-7</td><td>59.8±0.6</td><td>0.52</td></tr><tr><td>BUF6</td><td>Buffon</td><td>Fracture</td><td>Cal1</td><td>Zoned, bright to very dull red</td><td>-11.9±0.1</td><td>1.4±0.0</td><td>0.61±0.014</td><td>2</td><td>49±6</td><td>-5</td><td>56.1±2.4</td><td>0.73</td></tr><tr><td>ETR4</td><td>Etrochey</td><td>Moldic pore</td><td>Cal1</td><td>Uniform, very dull red</td><td>-10.1±0.1</td><td>2.5±0.0</td><td>0.639±0.02</td><td>2</td><td>38±7</td><td>-5</td><td>51.2±1.2</td><td>0.83</td></tr><tr><td>BUF4b<sup>e</sup></td><td>Buffon</td><td>Moldic pore</td><td>Cal1</td><td>Zoned, bright to very dull red</td><td>-10.3±1.6</td><td>0.3±0.4</td><td>0.642±0.021</td><td>3</td><td>37±7</td><td>-5</td><td>50.2±7.5</td><td>0.51</td></tr><tr><td>BUF11</td><td>Buffon</td><td>Fracture</td><td>Cal1</td><td>Uniform, very dull red</td><td>-12.1±0.1</td><td>2.0±0.0</td><td>0.611±0.007</td><td>2</td><td>48±3</td><td>-5</td><td>48.9±7.3</td><td>0.56</td></tr><tr><td>BUFcorail1</td><td>Buffon</td><td>Moldic pore</td><td>Cal2</td><td>Uniform, bright orange</td><td>-7.5</td><td>1.9</td><td>0.654</td><td>1</td><td>32</td><td>-3</td><td>—</td><td>—</td></tr><tr><td>BUFfracture</td><td>Buffon</td><td>Fracture</td><td>Cal2</td><td>Uniform, bright orange</td><td>-7.4±0.1</td><td>2.0±0.1</td><td>0.683±0.016</td><td>2</td><td>23±5</td><td>-5</td><td>41.6±1.4</td><td>0.87</td></tr><tr><td>BUF3b</td><td>Buffon</td><td>Fracture</td><td>Cal3</td><td>Uniform, dull red</td><td>-8.0±0.1</td><td>1.7±0.1</td><td>0.687±0.006</td><td>2</td><td>22±2</td><td>-6</td><td>19.0±4.1</td><td>0.58</td></tr><tr><td>ETR4</td><td>Etrochey</td><td>Moldic pore</td><td>Ded</td><td>Non-luminescent to bright orange</td><td>-7.2</td><td>-2.2</td><td>0.73</td><td>1</td><td>9</td><td>-8</td><td>1.9±3.5</td><td>0.83</td></tr></tbody></table>

Note: Values include δ<sup>18</sup>O, δ<sup>13</sup>C and Δ<sub>47</sub> compositions with associated uncertainties, number of replicates (n), precipitation temperatures (TΔ<sub>47</sub>), parent water δ<sup>18</sup>O<sub>w</sub> composition, U-Pb ages with uncertainties, and initial <sup>207</sup>Pb/<sup>206</sup>Pb ratios.

Error values are standard deviation of the mean.

aValues relative to the carbon dioxide equilibrium scale or CDES. An acid correction factor of 0.092% was applied to normalise these data to the 25°C phosphoric acid reaction scale (Henkes et al. 2013).

bTemperatures calculated using linear regressions through the theoretical Δ<sub>47</sub>-temperature relationship from Bonifacie et al. (2017).

cWater isotope compositions calculated using TΔ<sub>47</sub> and the calcite δ<sup>18</sup>O with the equation of O'Neil et al. (1969).

dIsochron intercept on the y-axis is the initial <sup>207</sup>Pb/<sup>206</sup>Pb ratio of the mineralizing fluid.

eThis sample was also analysed for δD and δO compositions of fluid inclusions by Dassié et al. (2018).
<figure><img src="image_4.png" /><figcaption>**FIGURE 2** | Petrographic plate illustrating the main microscopic features of the diagenetic carbonates investigated. To the left are plane polarised light images; to the right are the same images under cathodoluminescence (CL). (A) Cal1 cement filling a fracture in oolitic to peloidal grainstone and displaying a uniform to slightly zoned dull red CL. (B) Course equant blocky crystals of Cal2 filling a fracture with a very bright orange CL. (C) Cal3 cement filling a fracture in peloidal to oolitic packstone and displaying a uniform and very dull red CL. (D) Dedolomite crystal (Ded) preserving shimitar-like habitus of saddle dolomite occurs in a moldic pore and displays a bright orange to non-luminescent CL. The saddle dolomite was post-dated (prior to dedolomitization) by Cal1 cement that displays a rather uniform dull red CL. [Colour figure can be viewed at wileyonlinelibrary.com]</figcaption></figure>
<figure><img src="image_5.png" /><figcaption>**FIGURE 3** | Results of LA-ICP-MS U-Pb dating of carbonate diagenetic phases (Cal1, Cal2, Cal3, Ded). Multiple Cal1 samples, labelled from “a” to “g,” are ranked chronologically by their U-Pb ages. Tera-Wasserburg Concordia diagrams ($^{238}$U/$^{206}$Pb versus $^{207}$Pb/$^{206}$Pb) display the isotopic ratios for each phase, with lower intercept ages reported alongside $2\sigma$ internal errors. The grey-shaded areas represent the envelopes of the isochrons. MSWD stands for mean squared weighted deviates. [Colour figure can be viewed at wileyonlinelibrary.com]</figcaption></figure>

# 5 Discussion

## 5.1 | Origin of Diagenetic Carbonates

The diagenetic history of the Jurassic succession outcropping in the southeastern margin of the Paris Basin is poorly documented. To date, a single paragenetic sequence was reported for the *Oolithe Blanche* Formation in a nearby quarry (Makhloufi et al. 2013). This study, based on petrography only, identified different blocky calcite cements, precipitated from mesogenetic reducing fluids, followed by a planar-E dolomite that was subsequently dedolomitised during telogenesis.

More detailed investigations of the Jurassic succession were conducted towards the basin's eastern margin (e.g., Brigaud et al. 2009; André et al. 2010; Carpentier et al. 2014; Pisapia et al. 2018; Blaise et al. 2022) and the basin depocentre (e.g., Matray et al. 1989; Demars 1994; Worden and Matray 1995; Mangenot et al. 2017; Mangenot, Gasparrini, Rouchon, and Bonifacie 2018; Mangenot, Gasparrini, Gerdes, et al. 2018). These studies invoked meteoric recharges from different fluid source areas (e.g., London Brabant Massif, Ardennes Massif, the southeastern relief(s) to explain the origin of diagenetic carbonates formed during various uplift phases.

Cal1, Cal2, and Cal3 phases here investigated precipitated during the Tertiary from fluids with negative $\delta^{18}O_w$ (−5‰ to −7‰; Figure 4) pointing towards fluids with a meteoric signature. The meteoric origin of the fluids is also supported by direct isotope analyses of fluid inclusions in Cal1 (sample Buf4b

previously analysed by Dassié et al. (2018)), which revealed $\delta^{18}O_w$ and $\delta D$ of −6.6‰ and −31‰, respectively—values aligned with the global modern meteoric water line. The Ded phase formed during the Quaternary from fluids with the most negative $\delta^{18}O_w$ (−8‰) that mirrors the composition of present-day rainfall in Burgundy (−7‰ to −8‰, IAEA (2005); Figure 4). This phase formed under near-surface telogenetic conditions, as also indicated by the iron oxide precipitation (Figure 2D) due to $Fe^{2+}$ release and oxidation to $Fe^{3+}$ in an oxidising solution upon dedolomitisation (e.g., Nader et al. 2008; Schoenherr et al. 2018). In conclusion, the four diagenetic phases investigated document episodic meteoric water infiltrations from the southeastern basin margin, spanning from Palaeocene to Quaternary.

Interestingly, calcites with U-Pb ages overlapping those of Cal1 have been reported from the eastern margin (Blaise et al. 2022) and the basin depocentre (Mangenot et al. 2017; Mangenot, Gasparrini, Rouchon, and Bonifacie 2018; Mangenot, Gasparrini, Gerdes, et al. 2018), where they also precipitated from diluted fluids with meteoric affinity. This finding suggests that the documented meteoric recharge was a basin-scale process, driven by long-lasting regional hydrological connectivity over up to 60 My of uplift history.

## 5.2 | Exhumation History From $\Delta_{47}/U-Pb$ Carbonate Thermochronology

The ten T-t pairs determined by $\Delta_{47}/U-Pb$ thermochronology (Figure 5) were converted into burial depths using the
<figure><img src="image_6.png" /><figcaption>**FIGURE 4** | Temporal evolution of δ¹⁸O~w~ (A), δ¹⁸O (B), and Δ~47~ derived temperatures (C) as a function of U–Pb ages measured for each carbonate diagenetic phase (Cal1, Cal2, Cal3, Ded). The cross-plots illustrate progressive isotope and thermal evolution from burial diagenesis to near-surface conditions. Present-day rainfall δ¹⁸O~w~ composition (–7‰ to –8‰) and mean annual surface temperature (10°C–12°C) in the Burgundy region (IAEA 2005) are reported for comparison. [Colour figure can be viewed at wileyonlinelibrary.com]</figcaption></figure>

present-day mean surface temperature of 10°C–12°C and the most likely geothermal gradient of 30°C/km at the basin margins (Brigaud et al. 2009; Barbarand et al. 2013; Blaise et al. 2022). The resulting T–t-depth reconstruction (using T–t mean values for Cal1 samples) reveals two periods of exhumation and cooling (labelled 1 and 3 in Figure 5) occurring respectively between Cal1 and Cal2 (Palaeocene to Mid-Eocene) and between Cal3 and Ded (Early Miocene to Quaternary); they are separated by a phase of thermal stability (Mid-Eocene to Early Miocene; labelled 2 in Figure 5), during which temperature and depth

remained rather constant. The reconstructed T–t-depth path well reflects the known Pyrenean and Alpine compressional stages separated by extensional tectonics that are documented in the basin (Perrodon and Zabek 1990; Lacombe et al. 1990; Guillocheau et al. 2000). Furthermore, the T–t path data reflect the uplift dynamics modelled for the Bathonian-Callovian succession in the subsurface Parly well (Figure 5; thermal curve reported in Beaudoin et al. (2019) and extracted from the 3D numerical basin model detailed in Torelli et al. 2020), located 60 km WNW of our quarries (Figure 1). Despite differences in peak-burial and present-day temperatures (that are known to be higher in the subsurface compared to the outcrops; Ménétrier et al. 2005; Vergara Sassarini et al. 2023) and in curve steepness (which is expected to be higher at the basin margins where exhumation was more important; Barbarand et al. 2013), the reconstructed T–t path aligns with the modelled exhumation history (Figure 5). Further support for the robustness of the Δ~47~/U–Pb data comes from the seven T–t pairs for Cal1 overlapping with the beginning of basin inversion that post-dated the time of maximum burial for the studied succession (Late Cretaceous-Early Paleogene). The highest Cal1 precipitation temperatures (45°C ± 13°C, 48°C ± 3°C, 49°C ± 6°C; Table 1) correspond to thermal conditions typical of late diagenesis to early catagenesis of organic matter (Tissot and Welte 1984). These temperatures align with T~max~ values of 350°C–335°C from Rock Eval analyses on Lower Jurassic organic-rich mudrocks that underlie the studied succession, indicating the onset of the oil window (Uriarte 1997).

The exhumation history of the Paris Basin margins is debated. Most studies agree that the main uplift began in the Late Cretaceous to Early Paleogene, causing maximum exhumation and erosion at the southeastern and eastern margins, with lower exhumation in the southwestern margin and basin centre (Brunet and Le Pichon 1982). However, exhumation rate estimates are lacking in previous literature, and the total amount of eroded material remains a debated topic. In the southeastern part of the basin, estimates are primarily based on apatite fission-track analyses (Barbarand et al. 2013) from the Morvan Massif, that is the northernmost termination of the Massif Central (Figure 1), and that was once overlain by the basin sedimentary pile (Rat 1968). With the robustness of the Δ~47~/U–Pb data now demonstrated, our T–t-depth path can be used to estimate total erosion and cooling/exhumation rates related to the regional uplift affecting the Paris Basin from the Late Cretaceous onward. The minimum and maximum total erosions were calculated by considering the minimum and maximum precipitation temperatures of Cal1 and are 800 m and 1600 m, respectively. Using the mean precipitation temperature of Cal1 (43°C ± 5°C) an erosion of 1000 ± 200 m is estimated. These results are consistent with previous estimates (1300 ± 300 m; Barbarand et al. 2013) from the nearby Morvan Massif (Figure 1) and from the eastern basin margin (~1100 m; Blaise et al. 2022).

The calculated cooling and exhumation rates are as follows:

* Pyrenean compressional phase (Cal1–Cal2): 1.25°C/Ma and 37m/Ma.

* Quiescence period (Cal2–Cal3): 0.12°C/Ma and 3 m/Ma.
<figure><img src="image_7.png" /><figcaption>**FIGURE 5** | Thermal history (T-t path) of the studied succession based on Δ$_{47}$/U-Pb thermochronology data. The graph to the right shows the temperature (°C) versus time (Ma) and burial depth (m), with the key phases of exhumation labelled 1, 2, and 3. Phase 1 (Palaeocene to Mid-Eocene) corresponds to the Pyrenean compression, Phase 2 (Mid-Eocene to Early Miocene) represents a period of thermal stability linked to extension, and Phase 3 (Early Miocene to Quaternary) corresponds to the Alpine compression. The cooling/exhumation rates of each phase are also indicated. The graph to the left reports the same T-t dataset from Δ$_{47}$/U-Pb thermochronology as compared with the T-t path modelled for the Bathonian-Callovian succession at Parly well, located ~60 km to the WNW of the studied quarries (Figure 1). The modelled thermal curve of Parly well is from Beaudoin et al. (2019) and derived from the 3D numerical basin model detailed in Torelli et al. (2020). [Colour figure can be viewed at wileyonlinelibrary.com]</figcaption></figure>

• Alpine compressional phase (Cal3-Ded): 0.84°C/Ma and 25 m/Ma.

These data highlight that the Pyrenean compression transferred significant tectonic stress and had a stronger impact on exhumation compared to the geographically closer Alpine orogen.

## 6 | Conclusions

Four carbonate diagenetic phases from Middle Jurassic limestones exposed in the southeastern margin of the Paris Basin were analysed using Δ$_{47}$ thermometry and U-Pb dating to constrain precipitation conditions (temperature, time, δ$^{18}$O$_{w}$). The carbonates precipitated during Early Paleogene to Quaternary time—a period marked by significant uplift and denudation—from meteoric recharge fluids becoming progressively cooler and depleted in $^{18}$O. The temperature-time history reconstructed from these data reflects the basin tectono-thermal evolution and allowed calculating a total erosion of 1000 ± 200 m. Exhumation occurred at varying rates; it was faster during the Pyrenean compressional phase (37 m/ Ma) and slower during the Alpine compressional phase (25 m/ Ma). This study represents the first application of Δ$_{47}$/U-Pb

thermochronology to diagenetic carbonates for the reconstruction of uplift dynamics and exhumation rates in a sedimentary basin. The limited number of datapoints for the diagenetic phases may limit the robustness of the exhumation rate estimates; we therefore recommend that future applications rely on larger datasets if the available samples allow, since the large amount of carbonate powder needed for Δ$_{47}$ analyses may be a limiting factor.

This study is a significant contribution to basin analysis and demonstrates that the Δ$_{47}$/U-Pb thermochronology approach can be applied to carbonate-dominated successions elsewhere, filling gaps and reducing uncertainties associated with other low-temperature thermochronology methods.

## Acknowledgements

IFP energies nouvelles is thanked for funding the PhD of Xavier Mangenot (2014–2017) during which Δ$_{47}$ analyses were achieved. The research was successively supported by the Khalifa University of Science and Technology under the Award No. CIRA-2021-048 and by the Italian Ministry for Universities and Research (MUR) through the project "Dipartimenti di Eccellenza 2023-27". Fabrice Gaumet is warmly thanked for having illustrated to the first author
the sampled quarries during field trips in the frame of IFP-school
classes. Virgile Rouchon is thanked for his wise suggestions during
the doctoral research of Xavier Mangenot. Abel Guihou (CEREGE,
Aix-en-Provence, France) is thanked for his support on U-Pb
measurements on the ENVITOP platform. Two anonymous review-
ers and the associate editor Tomas Capaldi are thanked for their
constructive contribution. Open access publishing facilitated by
Università degli Studi di Milano, as part of the Wiley - CRUI-CARE
agreement.

Conflicts of Interest

The authors declare no conflicts of interest.

Data Availability Statement

The data that supports the findings of this study are available in the
*Supporting Information* of this article.

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## Supporting Information

Additional supporting information can be found online in the Supporting Information section. Data S1: ter70004-sup-0001-Supinfo.zip.