Insights into the Thermal History of North-Eastern Switzerland—Apatite Fission Track Dating of Deep Drill Core Samples from the Swiss Jura Mountains and the Swiss Molasse Basin

: This work presents new apatite ﬁssion track LA–ICP–MS (Laser Ablation Inductively Coupled Plasma Mass Spectrometry) data from Mid–Late Paleozoic rocks, which form the substratum of the Swiss Jura mountains (the Tabular Jura and the Jura fold-and-thrust belt) and the northern margin of the Swiss Molasse Basin. Samples were collected from cores of deep boreholes drilled in North Switzerland in the 1980s, which reached the crystalline basement. Our thermochronological data show that the region experienced a multi-cycle history of heating and cooling that we ascribe to burial and exhumation, respectively. Sedimentation in the Swiss Jura Mountains occurred continuously from Early Triassic to Early Cretaceous, leading to the deposition of maximum 2 km of sediments. Subsequently, less than 1 km of Lower Cretaceous and Upper Jurassic sediments were slowly eroded during the Late Cretaceous, plausibly as a consequence of the northward migration of the forebulge of the neo-forming North Alpine Foreland Basin. Following this event, the whole region remained relatively stable throughout the Paleogene. Our data show that the Tabular Jura region resumed exhumation at low rates in early–middle Miocene times ( « 20–15 Ma), whereas exhumation in the Jura fold-and-thrust belt probably re-started later, in the late Miocene ( « 10–5 Ma). Erosional exhumation likely continues to the present day. Despite sampling limitations, our thermochronological data record discrete periods of slow cooling (rates of about 1 ˝ C/My), which might preclude models of elevated cooling (due to intense erosion) in the Jura Mountains during the Miocene. The denudation ( « 1 km) of the Tabular Jura region and the Jura fold-and-thrust belt ( « 500 m) has provided sediments to the Swiss Molasse Basin since at least 20 Ma. The southward migration of deformation in the Jura mountains suggests that the molasse basin started to uplift and exhume only after 5 Ma, as suggested also by previous authors. The data presented here show that the deformation of the whole region is occurring in an out-of-sequence trend, which is more likely associated with the reactivation of thrust faults beneath the foreland basin. This deformation trend suggests that tectonics is the most determinant factor controlling denudation and exhumation of the region, whereas the recently proposed “climate-induced exhumation” mechanism might play a secondary role.


Introduction
A vast amount of research has been carried out to understand the geological evolution of the Swiss Jura Mountains (Jura fold-and-thrust belt and the Tabular Jura) and the Swiss Molasse Basin (SMB, also referred to as the North Alpine Foreland Basin, NAFB) in north-eastern Switzerland (Figure 1a,b). Published research includes detailed geological mapping [1,2], structural, sedimentological, and seismic coverage generated by various exploration companies and synthetized by several authors [3][4][5], as well as deep and shallow drilling reports [6][7][8][9][10][11].
Despite this long history of research and publications, there are still uncertainties on the timing of the main tectonic events and the amount of exhumation that likely accompanied these events. The main shortcomings are due to the lack of an accurate determination of the onset and duration of two of the most important deformational and erosional events observed in the region, which are represented by two regional unconformities: (i) the Jurassic-Eocene unconformity and (ii) the Miocene-Quaternary unconformity.
The Jurassic-Eocene unconformity observed in seismic images is arguably a consequence of the northward migration of the forebulge, as the proto NAFB formed and showing the different morphotectonic units that are discussed in the text. The map includes also subsurface data reported by [4].
Despite this long history of research and publications, there are still uncertainties on the timing of the main tectonic events and the amount of exhumation that likely accompanied these events. The main shortcomings are due to the lack of an accurate determination of the onset and duration of two of the most important deformational and erosional events observed in the region, which are represented by two regional unconformities: (i) the Jurassic-Eocene unconformity and (ii) the Miocene-Quaternary unconformity.
The Jurassic-Eocene unconformity observed in seismic images is arguably a consequence of the northward migration of the forebulge, as the proto NAFB formed and started to subside as a consequence of the uploading of the neo-forming Alpine Chain [12]. The timing of this erosional event has not been properly established, but it is considered to be Late Cretaceous-Middle Paleocene, as observed in the German part of the NAFB [13] or Paleocene [12,14]. The amount of pre-Eocene missing section has been estimated between 600 and 1800 m [14,15].
The Miocene-Quaternary unconformity is readily observed in the Jura fold-and-thrust belt (FTB), as well as in the entire SMB [15,16]. Some authors claim that the deformation of the Jura FTB started at around 12 Ma and lasted until about 5-4 Ma [17][18][19][20]. Synchronous deformation was recorded in the adjacent SMB [18], whose onset is debatably constrained between 10 [14,21] and 5 Ma [17,18,22,23]. While there have been no attempts to determine the amount of Miocene sedimentary section eroded from the Swiss Jura mountains, the thickness of the Miocene section missing in the SMB has been roughly estimated between 350 m and up to 3 km [14,15,22,23].
This work addresses some of the aforementioned standing problems: the timing and magnitude of exhumation due to the tectonic events in the Swiss Jura Mountains and in the adjacent SMB. To achieve this objective, we have employed apatite fission track dating from selected deep borehole cores, which were drilled in Northern Switzerland in the 1980s by Nagra (Swiss National Cooperative for the Disposal of Radioactive Waste) and that reached the crystalline basement.

Major Morphotectonic Units in Northern Switzerland
In northern Switzerland, the Paleozoic crystalline basement of the Black Forest Massif (Figures 1b and 2) is unconformably overlain by a series of Permo-Carboniferous to Jurassic sedimentary units usually referred to as the Tabular Jura (or the Plateau Jura). The Tabular Jura is considered autochthonous, and it is bounded to the south by the Jura FTB, which is a thin-skinned belt of Mesozoic sedimentary units ( Figure 2).  2] showing the different tectonic and sedimentary units, as well as the location of boreholes studied in this work. The structural elements include also subsurface data reported by [4]. The possible extent of the buried Paleozoic Constance-Frick Trough is shown with a dotted pattern (after [4]

Stratigraphic Evolution
At the end of the Variscan orogeny, strike-slip transpression controlled the formation of a series of long, narrow (5 km to 20 km) and relatively deep (up to 6 km; [4,29]) troughs, which are currently only observed in seismic lines, gravity data, or penetrated by a few deep wells [4,20,[29][30][31]. These troughs were filled by Permo-Carboniferous continental sediments that were likely buried and heated at elevated geothermal gradients (up to 100 °C/km; [14,15,32]) as a response to crustal thinning and magmatic underplating following the Variscan orogeny [33]. For instance, a well-described Permo-Carboniferous trough in north-eastern Switzerland is the Constance-Frick Trough (CTF; Figure 2), which started  2] showing the different tectonic and sedimentary units, as well as the location of boreholes studied in this work. The structural elements include also subsurface data reported by [4]. The possible extent of the buried Paleozoic Constance-Frick Trough is shown with a dotted pattern (after [4] Both the Tabular Jura and the Jura FTB form the Jura Mountains in northern Switzerland and are considered the most external deformation zone of the Alps [24] (Figure 1a). The Jura FTB probably detached from basement along Triassic evaporite layers [20,25,26] during the last phases of alpine deformation in Miocene times [18].
The SMB located between the northern flank of the Alps and the Jura Mountains is an early Oligocene-late Miocene peripheral foreland basin. The SMB is mainly undeformed with the exception of the Subalpine Molasse Unit, which is the external part of the Alpine thrust wedge. Mild deformation occurs also along isolated faults and folds [27] or near the margins of the basin, close to the Alps and the Jura Mountains [28].

Stratigraphic Evolution
At the end of the Variscan orogeny, strike-slip transpression controlled the formation of a series of long, narrow (5 km to 20 km) and relatively deep (up to 6 km; [4,29]) troughs, which are currently only observed in seismic lines, gravity data, or penetrated by a few deep wells [4,20,[29][30][31]. These troughs were filled by Permo-Carboniferous continental sediments that were likely buried and heated at elevated geothermal gradients (up to 100˝C/km; [14,15,32]) as a response to crustal thinning and magmatic underplating following the Variscan orogeny [33]. For instance, a well-described Permo-Carboniferous trough in north-eastern Switzerland is the Constance-Frick Trough (CTF; Figure 2), which started to subside in Late Carboniferous times, reaching maximum depth during Early Permian [4].
The Late Permian/Early Triassic was characterized by a long-term rift-related thermal subsidence [32], which regionally led to the opening of the Tethys Ocean. In Central Europe, this was followed by marine sedimentation during the Middle Triassic in an epicontinental sea environment [34] that lasted at least until the latest Jurassic. During the Jurassic-Cretaceous, the geothermal gradients were cooler (30-50˝C/km) when compared to the Permo-Carboniferous ones [15].
Although the contact Jurassic-Eocene appears to be conformable on seismic lines, there is a major disconformity between the youngest preserved Jurassic sediments and their overlying Eocene sediments in the north-eastern SMB and the Jura FTB. This important gap in the depositional record has led several authors to propose that a major erosional event occurred prior to Eocene times [13,35]. Most authors believe that deposition occurred throughout the Cretaceous, and it is now missing [14,15,36] in north-eastern Switzerland.
Eocene and younger sedimentation in the SMB developed into two main wedgeshaped cycles of shallowing upward deposition. The entire sequence comprises the early underfilled Lower Marine and Lower Freshwater units (UMM and USM, respectively using German acronyms) followed by the overfill deposition of the Upper Marine and Upper Freshwater molasses (OMM and OSM, respectively). The total sedimentary thickness was variable across the basin reaching several kilometers close to the alpine front [15].

Some Important Tectonic Structures in the Region
As previously mentioned, one of the best-known Late Paleozoic troughs is the Constance-Frick Trough [4,37,38], which is seismically defined as a low-angle half graben. The Constance-Frick Trough extends beneath the present-day Cenozoic molasse basin north of Zürich and extends westwards beneath the Tabular Jura possibly straddling the border of the Jura FTB through the Jura Main Thrust [4] (Figure 2). The northernmost limit of the Constance-Frick Trough is the seismically-defined Mandach Fault (Figure 2), which is a steeply dipping normal fault that was inverted in Late Neogene times [4]. The Mandach Fault probably extends at depth as a listric detachment fault [4].
The faults bordering the Late Paleozoic troughs were probably reactivated during Early Jurassic extension [34]. The Constance-Frick Trough border faults most likely also played a major role in the compressive Miocene deformation observed in the area, and they were probably reactivated during the Late Neogene Alpine orogeny [4,20].

Published Thermochronological Work-Conflicting Thermal Histories on the Basin
Existing thermal histories in the SMB have been mostly constrained by vitrinite reflectance and apatite fission track (AFT) data from core samples collected from deep wells throughout the basin [14,17,39] and from surface sedimentary samples [40]. The thermal histories proposed by these works show contrasting solutions.
One of the most referenced works in the region is [14], which included a series of AFT data obtained commercially by Nagra in the early 1990s [41]. The results (obtained from borehole samples) presented by [14] showed a complex basin evolution with high geothermal gradients in Permo-Carboniferous times followed by modest erosion (<1 km) during the Permian. This erosional period was followed by Mesozoic deposition, on which the lowermost deposits reportedly reached up to 100˝C by the end of the Cretaceous. Milder geothermal gradients (30-50˝C/km) were probably present throughout the Mesozoic. Interpretations by [14] suggested that erosion (removal of 600-700 m of Jurassic and Cretaceous sediments) was responsible for Late Cretaceous-Paleocene cooling. In turn, Miocene molasse sedimentation was responsible for variable heating across the basin. Finally, the SMB was inverted during late Miocene and part of the Miocene molasse section was reportedly eroded (estimates between 750 and 1050 m).
However, a closer look at AFT thermal models by [14] suggests that the whole Mesozoic section was almost completely exhumed ( Figure 3), and the basement rocks reached near-surface temperatures by the Late Cretaceous (see for instance Benken borehole data [14]). The best-fit forward model for the Benken well in [14] (location shown in Figure 2) calls also for a slow Cenozoic heating event (reaching about 90˝C in the late Miocene) followed by latest Miocene cooling. AFT thermal history interpretations by [14] are admittedly complicated because they call for rapid changes in lithospheric heat flow coupled with the thermal effects of burial and erosion.
A completely different thermal history than that of [14] for the same Benken borehole (and same depth) was obtained by a different author [17]. The latter thermal history rather suggested an important Late Jurassic/Early Cretaceous cooling event followed by isothermal conditions throughout most of the Cretaceous-early Cenozoic and followed by an important heating event from Late Eocene through Miocene ( Figure 3).
Other examples of dissimilar thermal models were presented by [39] on the same wells (Kaisten, Riniken, Leuggern, Siblingen; locations shown in Figure 2) analyzed by [14]. Although the AFT ages from the same wells were roughly similar within error, the thermal models obtained by [39] suggested two extremely fast Early Cretaceous (cooling) and Eocene (heating) events ( Figure 3). The unreported fast Eocene heating event was ascribed by [39] to represent hydrothermal fluid circulation during Eocene times.  Figure 2). All paths represent the best-fit inverse model with the exception of Benken, which is either a forward model (red line [14,41]) or a good-fit solutions envelope (yellow area, [17]). All previously published AFT data were obtained by the external detector method or by the multi-grain population method.
The evident discrepancies on the thermal models from boreholes of the same region [14,17,39] clearly leave us with doubts regarding the actual thermal history of the basin. In this respect, most of the discrepancies between the published AFT thermal models might be explained by several analytical reasons: (i) Key parameters used for apatite thermal modelling, which are currently standard practice, were not included in some of the previous publications such as kinetic proxies  Figure 2). All paths represent the best-fit inverse model with the exception of Benken, which is either a forward model (red line [14,41]) or a good-fit solutions envelope (yellow area, [17]). All previously published AFT data were obtained by the external detector method or by the multi-grain population method.
The evident discrepancies on the thermal models from boreholes of the same region [14,17,39] clearly leave us with doubts regarding the actual thermal history of the basin. In this respect, most of the discrepancies between the published AFT thermal models might be explained by several analytical reasons: (i) Key parameters used for apatite thermal modelling, which are currently standard practice, were not included in some of the previous publications such as kinetic proxies (e.g., Cl, Dpar) or annealing anisotropy corrections (e.g., c-axis projection).
(ii) Some of the publications [14] included mainly "forward" modeling leaving, most AFT data unextracted, as opposed to most modern and computer-intensive "inverse" modeling.
(iii) Thermal models from previous publications [14,39] were derived using an AFT annealing model [42] that is known for providing spurious late cooling events, which usually lead to an over interpretation of a kilometer or more of unroofing. The latter cooling is usually considered a modeling artefact with no geological significance (see discussion in [43]).
(iv) The recent annealing models for thermal history inversion are based on more extensive laboratory annealing experiments than their older counterparts (see discussion in [44]).
For these reasons, we acquired new AFT data using a state-of-the-art LA-ICP-MS (Laser Ablation Inductively Coupled Plasma Mass Spectrometry) analytical approach (see below) using the latest thermal annealing model available [44] in order to quantitatively determine the amount of cooling and heating during the Meso-Cenozoic time period.

Sampling
Pre-Triassic units were sampled from borehole cores ( Figure 2) collected from the Swiss Geological Survey (Swisstopo) core repository, located in Hochdorf (Canton of Luzern). The wells analyzed form part of a Nagra drilling campaign (carried out between 1983 and 1984), which aimed to characterize the crystalline basement in order to evaluate the feasibility of nuclear waste repository [6][7][8][9][10][11]. The stratigraphic sections for each well are shown in Figure 4. All samples were collected from depths between 658 and 2238 m and include: (a) Mid-Late Paleozoic granitoids and metasediments in the Böttstein, Kaisten, Leuggern, Weiach, and Schafisheim wells, which were sampled immediately below the major Mesozoic unconformity ( Figure 4).

Methods
Apatite fission track (AFT) thermochronology provides quantitative thermal history information between «120 and 60˝C, corresponding to the upper 2-4 km of the crust depending on the geothermal gradient [45]. Apatite fission tracks partially anneal within the apatite partial annealing zone (APAZ), which has been defined by both laboratory time-scale experiments and field observations [46]. Thus, track annealing kinetics and the temperature bounds of the APAZ are also a function of apatite composition [47,48].
AFT age data were acquired by the Laser Ablation Inductively Coupled Plasma Mass Spectrometry (LA-ICP-MS) approach at the University of Geneva and the University of Lausanne in an identical approach to [49,50]. Natural fission tracks crossing the polished apatite grains surface were etched for counting using: 5.5 N HNO 3 for 20.0 (˘0.5) seconds at 21.0˝C with a high-precision water bath. Mounts were scanned to search for the best apatite grains for age dating and grain location, and pictures were digitally recorded with a high-resolution camera for potential reinvestigations. Spontaneous fission tracks were counted on-screen, using a Microscope Zeiss Axio-Imager.z1, which is digitally connected to a high-resolution screen.
Grain localities were further revisited using a LA-ICP-MS facility (an Element XR sector-field ICP-MS interfaced to a Resolution 193 nm excimer ablation system equipped with an S155 two-volume ablation cell) at the University of Lausanne in order to determine 238 U concentrations and other elemental compositions. The analyses used a single laser spot (laser spot size was kept constant during all sessions at 38 µm). The cylindrical pit was excavated to a depth beyond which uranium did not contribute fission tracks to the etched grain surface (the depth of the pit was about 7 µm). We used SRM612 as primary reference material for trace element composition. The raw elemental data were reduced using LAMTRACE, using only SRM612 glass as the primary trace element abundance standard. 42 Ca served as an internal standard (all extra analytical details, as well as age calculations are described in [51].

Methods
Apatite fission track (AFT) thermochronology provides quantitative thermal history information between ≈120 and 60 °C, corresponding to the upper 2-4 km of the crust depending on the geothermal gradient [45]. Apatite fission tracks partially anneal within the apatite partial annealing zone (APAZ), which has been defined by both laboratory timescale experiments and field observations [46]. Thus, track annealing kinetics and the temperature bounds of the APAZ are also a function of apatite composition [47,48]. Potential thermal history solutions are derived by inverse modelling the AFT age data, track lengths, and compositional data using the HeFTy ® software (v.1.9.3) [52]. We used Dpar (mean maximum diameter of fission track etch figures parallel to the crystallographic c-axis) [53] as a proxy for the apatite chemistry required for the multi-compositional annealing algorithms. The inverse modelling is a controlled random search procedure that predicts thermal history paths that closely match the observed AFT analytical data. The procedure was performed using the annealing algorithm of [44].

AFT Ages and Length Results
Sample details and AFT data from the Tabular Jura mountains (Böttstein, Kaisten, Leuggern wells), the Jura FTB domain (Riniken, Weiach wells), and from the SMB (Schafisheim well) are shown in Table 1 and Figure 4. AFT ages obtained from the Tabular Jura mountains samples range from 35

AFT Modeling Constraints
In the absence of a reliable and comprehensive bottom hole temperature (BHT) data set to determine the present-day temperature required by the modeling, we have modeled the AFT data assuming a regional present-day geothermal gradient of 35˝C/km and an average surface temperature of 15˝C. The assumed geothermal gradient is in line with existing well temperature data, and it is also within the expected range for stable continental areas. Present-day temperature gradients for the Riniken, Kaisten, and Leuggern wells is in the order of 35˝C/km below shallow depths of 300 m [8][9][10]. The Schafisheim well has an average gradient of 37˝C/km for depths below 1000 m [11]. The Böttstein well has a geothermal gradient of 34˝C/km measured along the whole crystalline section [6]. The Weiach well has reportedly an average 41˝C/km (although with a highly scattered determination; [7]).
Nonetheless, the inverse modeling performed with HeFTy ® included a relatively open (˘10˝C) present day-temperature value at the appropriate sample depth in order to account for possible uncertainties. Goodness of fit parameters, which indicate the fit between measured length distribution and the modeled data, resulted in values close to 1. Our interpretations are based upon the best-fit model, the good-fit, and acceptable-fit envelope of solutions yielded by the thermal models (see Figure 5).  [58] and 1 measurement by [59]). Equivalent isotropic track length: 16.2 µm. Figure 5. Thermal history models for the different regions. Eight samples were modeled using the software HeFTy ® (version 1.9.3). Input data included AFT age, track length data, and Dpar (a proxy for chemical composition). The thermal constraints in the time-temperature window for the inverse modeling are (i) basement rocks required to be at surface levels by Late Permian-Early Triassic times, and (ii) present-day (time = 0 Ma) temperature calculated by the total depth (TD) of the sample and the assumed present-day geothermal gradient (see Table 1). Note similar thermal models' patterns for samples from the same well located at different depths. The best-fitting and the weighted mean paths are shown as solid dark blue and black lines, respectively. The good-fit envelope of solutions (all solutions with a goodness of fit of 0.5 and higher) are shown in pink. Acceptable solutions (goodness of fit between 0.05 and 0.5) are shown in green.
We also modeled samples from the same well in parallel assuming continuous burial between samples that are not separated by unconformities, following the approach of [60]. Results are shown in Figure 6A and correspond to samples @1144 m and @1796 m for Riniken and samples @1899 m and @1944 m for Weiach. Although the modeling did not yield good solutions fitting all data, the simultaneous modeling shows a wider acceptable solution range, with the best-fit solution following roughly the same path observed in Figure 5 (single-sample modeling). This wider acceptable range of the combined inversion broadens possibilities of Miocene heating and cooling but still rules out extreme events of heating and cooling. Figure 5. Thermal history models for the different regions. Eight samples were modeled using the software HeFTy ® (version 1.9.3). Input data included AFT age, track length data, and Dpar (a proxy for chemical composition). The thermal constraints in the time-temperature window for the inverse modeling are (i) basement rocks required to be at surface levels by Late Permian-Early Triassic times, and (ii) present-day (time = 0 Ma) temperature calculated by the total depth (TD) of the sample and the assumed present-day geothermal gradient (see Table 1). Note similar thermal models' patterns for samples from the same well located at different depths. The best-fitting and the weighted mean paths are shown as solid dark blue and black lines, respectively. The good-fit envelope of solutions (all solutions with a goodness of fit of 0.5 and higher) are shown in pink. Acceptable solutions (goodness of fit between 0.05 and 0.5) are shown in green.

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Metasedimentary basement samples from the Tabular Jura region (Böttstein, Kaisten, and Leuggern wells): All the basement rocks dated from this region are overlain by non-metamorphosed Triassic sediments (Figure 4), meaning that they were exposed at the surface at least toward the end of the Permian. The good-fit solutions suggest that these samples were heated continuously from Late Permian until the Early Cretaceous to temperatures close to 100˝C ( Figure 5). Thus, the basement rocks immediately underlying the Mesozoic sediments were never heated above 120˝C (corresponding to the total annealing zone). The thermal models suggest a very slow Late Cretaceous cooling (100 Ma to 70 Ma) from 100˝C to about 80-70˝C at rates of «1˝C/My. In addition, the good-fit models ( Figure 5) suggest that these samples roughly stayed at isothermal conditions throughout the early Cenozoic and were finally slowly cooled at around 20-15 Ma (early-mid Miocene) from 70˝C until present-day well temperatures («50˝C).

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Sedimentary and crystalline basement samples from the Jura FTB (Riniken and Weiach wells): In these wells, both Permo-Carboniferous sediments and older crystalline basement rocks were sampled (Figure 4). The AFT models show that all samples were continuously heated from Permian to Early Cretaceous («100 Ma) until temperatures were between 80 and 100˝C ( Figure 5). An episode of very slow cooling, Late Cretaceous (100 to 80 Ma) in age, was observed in the Riniken well, where samples cooled from 90 to about 70˝C at rates as low as 1˝C/My.
The good-fit thermal solutions show more or less isothermal conditions for most of the Cenozoic. A net drop in temperature by a «10˝C (final temperatures depending on the well) is recorded after 10 Ma. This late Miocene cooling postdates onset of cooling observed in the Tabular Jura region (early-mid Miocene).

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Granitoids flooring the SMB s.s. (Schafisheim well): No samples from granitoid rocks yielded enough AFT data for a robust AFT thermal modeling of the basement flooring the SMB.
We also modeled samples from the same well in parallel assuming continuous burial between samples that are not separated by unconformities, following the approach of [60]. Results are shown in Figure 6A and correspond to samples @1144 m and @1796 m for Riniken and samples @1899 m and @1944 m for Weiach. Although the modeling did not yield good solutions fitting all data, the simultaneous modeling shows a wider acceptable solution range, with the best-fit solution following roughly the same path observed in Figure 5 (single-sample modeling). This wider acceptable range of the combined inversion broadens possibilities of Miocene heating and cooling but still rules out extreme events of heating and cooling.
For visualization purposes and to increase robustness, we have grouped and remodeled all the AFT age and length data from samples of the same boreholes (Figure 6b). Samples possibly correspond to the same geological units (no missing section between samples). The results for wells Weiach and Riniken in the Jura FTB are shown in Figure 6b, and their integrated thermal models do not differ substantially from the single-sample models ( Figure 5). The integrated results show that despite the limited amount of data, the complex thermal history (with extreme heating and cooling events) suggested by previous authors is probably not accurate. For visualization purposes and to increase robustness, we have grouped and remodeled all the AFT age and length data from samples of the same boreholes (Figure 6b). Samples possibly correspond to the same geological units (no missing section between samples). The results for wells Weiach and Riniken in the Jura FTB are shown in Figure  6B, and their integrated thermal models do not differ substantially from the single-sample models ( Figure 5). The integrated results show that despite the limited amount of data, the complex thermal history (with extreme heating and cooling events) suggested by previous authors is probably not accurate.

Interpretation of the Thermal History
The AFT thermal models of basement rocks in the Tabular Jura and Jura FTB areas provide significant information on the thermo-tectonic history of the region. Herein, we assume that heating is mainly driven by sedimentary burial and cooling caused by erosional exhumation. We use the term erosional exhumation to mean vertical upward movement of rocks with respect to the Earth's surface, representing a reduction of overburden due to erosion. Changes in lithospheric heat flow following the thinning of the lithosphere for rifting can be also a factor controlling basement temperature [61-63], Figure 6. (a) Simultaneous thermal histories for Weiach and Riniken wells following the approach of [60]. (b) Thermal models that integrate samples from the same boreholes (Weiach and Riniken) that do not have a missing section between them. The best-fitting and the weighted mean paths are shown as solid dark blue and black lines, respectively. The good-fit envelope of solutions (all solutions with a goodness of fit of 0.5 and higher) are shown in pink. Green areas are histories with acceptable fits (goodness of fit between 0.05 and 0.5).

Interpretation of the Thermal History
The AFT thermal models of basement rocks in the Tabular Jura and Jura FTB areas provide significant information on the thermo-tectonic history of the region. Herein, we assume that heating is mainly driven by sedimentary burial and cooling caused by erosional exhumation. We use the term erosional exhumation to mean vertical upward movement of rocks with respect to the Earth's surface, representing a reduction of overburden due to erosion. Changes in lithospheric heat flow following the thinning of the lithosphere for rifting can be also a factor controlling basement temperature [61][62][63], as suggested by previous authors for the Mesozoic rifting events registered in the SMB substratum [14,15,64]. Unfortunately, this cannot be constrained by our dataset, and we take our Early Mesozoic cooling/heating rates as maximum exhumation/burial estimates. In the absence of more reliable constrains for Early Mesozoic, we consider the paleo-geothermal average gradient of 40˝C/km proposed by [15] as a maximum estimate (see below).
Lithospheric heat flux changes in temperature probably did not impact significantly the latest Cretaceous-Cenozoic part of the history once Early Mesozoic rifting ended. Therefore, constant normal geothermal gradient between 30 and 25˝C/km is used to convert cooling into exhumation during the Latest Cretaceous-Cenozoic.
Although the Weiach well shows an important record of Carboniferous sediments (>500 m), herein below, we are interested in the Late Permian and younger part of the thermal history.

Latest Permian to Early Cretaceous Burial in the Tabular Jura and Jura FTB
The thermal histories of the basement yielded by the AFT models ( Figure 5) show a continuous heating (differential heating of more than «70˝C) that is consistent with a continued sedimentation from Late Permian to Early Cretaceous.
The maximum preserved thickness of Permian to Jurassic sediments is found in the Riniken and Weiach wells (up to 1.7 km; Figure 4), which are located along the Paleozoic Constance-Frick Trough. In all the other wells, only a few hundred meters or a complete absence of Permian deposits is observed, whereas Triassic to Jurassic preserved deposits range from 100 to 300 m (Böttstein, Kaisten, Leuggern wells) to 1000 m (Schafisheim well) (Figure 4). The preserved thickness of Permian to Upper Jurassic sediments clearly does not account for the observed heating (differential heating of «70˝C), meaning that the original section should have been thicker and/or the geothermal gradients operating during that time should have been higher. Although [15] suggested that Mesozoic prevailing geothermal gradients averaged 40˝C/km, we prefer a more conservative estimate of 30-35˝C/km, given that rift-related setting had already ceased by the Middle Triassic. Therefore, we estimate that about 2 km of sediments were deposited during this time period over most of the region.

Late Cretaceous Exhumation in the Tabular Jura and Jura FTB
The Late Cretaceous cooling from «100 to 80˝C between 100 and 80 Ma is observed in most of the wells, in particular in Tabular Jura. This cooling event can be related to the erosional exhumation and removal of part of the Lower Cretaceous/Jurassic section. In this case, by considering a Late Cretaceous geothermal gradient of 30˝C/km, such slow cooling rates (up to 1˝C/My) imply a removal of 1 km of the sedimentary pile during the 100 and 80 Ma time interval.

Early-Mid Cenozoic Burial History in the Tabular Jura and Jura FTB
The thermal history of the basement rocks in the region supports relatively stable conditions throughout most of the Cenozoic. This implies that a reduced sediment thickness was deposited on the Jura mountains area during this period. This is somehow reflected in the present day-sections of the Riniken, Kaisten, and Leuggern wells, where a reduced thickness of Cenozoic deposits is preserved (less than 100 m, Figure 4).

Miocene Exhumation in the Tabular Jura and Jura FTB
In the Miocene, a net cooling ranging between 10 (Jura FTB) and 20˝C (Tabular Jura) is observed in the Jura Mountains samples, and we ascribe this cooling to uplift and exhumation. Our thermal models show that cooling in the Tabular Jura region started in early-middle Miocene times (between 20 and 15 Ma), whereas cooling in the Jura FTB started in the latest Miocene (between 10 and 5 Ma), and it seems to be continuing today based on the cooling paths.
This early-late Miocene cooling and exhumation imply a further removal of «1000-700 m and «500-300 m of sediments in the Tabular Jura region and the Jura FTB, respectively. The material removed was arguably the very thin Cenozoic molasse section and-more probably-part of the remaining Lower Cretaceous and Jurassic sediments.

Jurassic-Eocene Unconformity and the Missing Mesozoic Sedimentary Section
Based on indicators such as porosity, vitrinite reflectance, and fission track dating, the amount of missing Mesozoic section for most of north-western Switzerland has been constrained between 600 and 1800 m in thickness by [15], 600-700 m by [14], or 3000 m by [65]. In the Zürich (High) area, an erosion of only about 600 m (consisting of 400 m of Upper Jurassic and 200 m of Cretaceous sediments eroded) has been estimated [15]. The large range of the erosion values estimated by previous authors probably comes from the uncertainties in the modeling procedure, as well as from the assumed paleogeothermal gradient.
On the other hand, our estimates suggest that the first exhumation event observed in the Tabular Jura and Jura FTB occurred in the Late Cretaceous and involved the removal of a maximum of 1 km of sedimentary section, which is in line with estimates made by [15]. The widespread Jurassic-Eocene unconformity was most likely a consequence of the northward migration of the forebulge, as the NAFB started to subside [12]. This early phase of Alpine development was arguably contemporaneous with the Subhercynian intraplate deformation observed in Central Germany [66].

Miocene Erosion and Tectonics of the Jura Mountains
The main deformation in the Jura FTB reportedly started between 15 and 12 Ma [18,20,28,[67][68][69] and lasted until about 5-4 Ma [19,20], although a few authors [70] suggest-based on geodetic evidence-that slow uplift of the Jura FTB is still ongoing.
Our data suggest that erosional exhumation of the Tabular Jura and the Jura FTB started at around 20 and 10 Ma, respectively. The Tabular Jura experienced the removal of maximum «1 km of overburden, while the Jura fold-and-thrust belt had a net reduction of only «500 m of sedimentary thickness throughout the Miocene.
We observe that the deformation and exhumation of the Jura mountains have migrated toward the hinterland throughout most of the Miocene. Therefore, the Black Forest Massif is possibly acting as a frontal buttress that hampers forward propagation, while it is possibly also being subtly uplifted. Although an earliest Miocene exhumation of the Black Forest Massif was probably localized in the Upper Rhine Graben shoulders [71], a lithosphericscale uplift in the Vosges-Black Forest arch (Figure 1a) has been constrained to occur since 18 Ma [72,73], which is coincident with our timing for the onset of deformation in the Tabular Jura region. Existing paleogeographic reconstructions [74] also suggest that by mid-Burdigalian times («18 Ma), the Vosges-Black Forest arch and the southern part of the Upper Rhine Graben started to supply detrital material to the SMB.
The deformational trend (starting at 20 Ma in the Tabular Jura/Black Forest Massif and 10 Ma in the Jura FTB) seems to indicate that probably major tectonic limits (e.g., the Mandach Fault) separating the Tabular Jura from the Jura FTB have played a role in the latest Miocene deformation observed in the region. The onset of the Jura FTB deformation, uplift, and exhumation («10 Ma) likely represent the timing when the Jurassic sequence detached from basement along Triassic evaporite layers [20,25].
Our thermochronological data indicate that uplift and exhumation of the Jura FTB might still be occurring although at very low rates, as corroborated by earthquake activity [75]. This differs from [18] on their view that uplift and deformation of the Jura FTB ended at 5 Ma.

Miocene Sedimentation and Subsequent Erosion in the Swiss Molasse Basin
The lack of AFT length data prevents us from determining the onset of exhumation of the SMB area during the Miocene. Although the youngest preserved sediments in the SMB are Tortonian in age (ca. 11 Ma; [76]), it is believed that sedimentation lasted until 5 Ma [19,22,23] or until 10 Ma [14].
Pinch-out geometries may attest that sedimentation in the SMB was partially synchronous with deformation of the Jura FTB, and the molasse deposits likely rode "piggyback" style above the Jura décollement as suggested by previous authors [18].
Sedimentation in the SMB was followed by uplift and erosional-driven exhumation [77]. The timing of the exhumation is poorly constrained, but it has been ongoing since 10 Ma [14,21] or-most likely-since 5 Ma [17,18,22,23]. The general southward-younging deformation trend observed in our data from the Jura mountains suggests that the onset of deformation of the SMB might have occurred at 5 Ma.
The amount of molasse sediments that eroded during the late Miocene exhumation event is poorly known, but it was certainly variable along and across the SMB. Based on stratigraphy and thermal indicators from well data, [15] estimated elevated amounts of erosion (up to 2.5 km) in the south-western part of the basin (e.g., Geneva area) with modest values (about 350 m) in north-eastern Switzerland (e.g., Zürich area). These values differ from those constrained by [14] in northernmost Switzerland, which are in the order of 750 and 1050 m. A post-5 Ma erosion and denudation south of Zürich of around 1.5 km was constrained by [17], while [22,23] estimate a missing section of about 1 km in the plateau south of Zürich and 2-3 km in the subalpine molasse regions. Summing up, the sedimentary thickness eroded during the Miocene in the SMB has been estimated to range from 350 to 3 km, depending on the distance from the Alpine Chain.
The low (<1 km) Miocene exhumation estimated by our data in the Jura mountains suggest conservative values also for the eroded material in the SMB, which are probably in the order of only a few hundred meters near the region of Zürich (similar to values proposed by [15]). As mentioned previously, some of the elevated exhumation values proposed by previous authors were probably an artefact of the thermal modelling procedure.

Main Drivers of the Miocene Uplift
The Late Cenozoic uplift and exhumation event is considered a consequence of deepseated mechanisms such as isostatic rebound due to the diminution or termination of downwelling of mantle material beneath the Alps [78], tectonic underplating [75], or mantle delamination [79]. Alternative shallower mechanisms suggest that erosion in the SMB accelerated due to an increased material flux from the Alps, which in turn was induced by humid conditions at the end of the late Miocene glacial period [80]. Most recent models [18,23] highlight the importance of climate-triggered erosion of the Swiss Alps producing rebound and exhumation of the entire Swiss foreland regions.
The regional trend of exhumation observed by our data-with uplift starting in the Tabular Jura and migrating southwards toward the Jura FTB-would suggest that uplift occurs in an out-of-sequence fashion, leading to a delayed erosion of the SMB when compared to northern regions. Out-of-sequence thrusting derived from our data has also been suggested to operate in the subalpine region and south-western part of the SMB in the Geneva area [75].
Although Cenozoic climatic changes probably played an important role in erosion [18,23], deeper tectonic processes involving the reactivation of major detachment faults (e.g., Mandach Fault) might be the main factor responsible for the deformation and uplift observed in the region. Therefore, early-late Miocene uplift of the Jura mountains is ultimately a consequence of increased uplift of the external Alpine massifs that transferred deformation through thrust faults beneath the foreland basin.

Further Implications for Basin Modeling and Natural Resources Exploration
The new data shed light on the depositional and erosional history of the region, including the tectonic activity of major bordering faults. Our data show that all the samples experienced a long history (>220 My) of heating and cooling, which was likely due to burial and exhumation processes, confirming some of the most conservative Jurassic-Early Cretaceous erosion estimates [15]. We believe that any future work should seek a more robust determination of the thermal histories than the one presented here by means of increased sampling through the borehole column, improved AFT length statistics (probably irradiating apatites with Cf particles to increase the revelation of more confined tracks), and the use of other thermochronometers such as U-Th/He. Nevertheless, our findings improve the reconstruction of the thermal history of the northern sector of the NAFB, in particular refining the timing and the potential maximum paleo-temperature that were attained by its sedimentary units. The new thermochronological dataset also allows us to calibrate thermal models that integrate vitrinite reflectance (VR) in the same region [81,82]. This integration of VR and AFT allowed [83] better estimating the amount of erosion for the main unconformities recognized in the basin, as well as the maximum burial depth of the main stratigraphic units. Overall, the new VR and AFT data are fundamental to evaluate the maturity of hydrocarbon source rocks, as well as evaluate the risk for geothermal exploration associated to hydrocarbon manifestations in the subsurface [82]. Ongoing collaborative works [82][83][84] are addressing issues of potential generation and circulation of hydrocarbon fluids that may represent a risk for the safety of nuclear waste repository envisaged for this area [85][86][87][88] and, eventually, for future deep geological CO 2 storage.

Conclusions
Despite sampling limitations, the new apatite fission track LA-ICP-MS data presented here provide valuable information on the post-Late Paleozoic history of the region, a long period of time in which the apatite fission track ages were never fully reset.
Permo-Carboniferous sedimentation occurred almost exclusively along the Constance-Frick Trough. Subsequent widespread Lower Triassic to Lower Cretaceous sedimentation occurred throughout the region, leading to the deposition of maximum 2 km of sediments. Part of the Lower Cretaceous and the Upper Jurassic sediments were subsequently eroded during the Late Cretaceous, from 100 to 70 Ma. This very slow erosional event was responsible for the conspicuous post-Jurassic unconformity observed in the whole area, and it was arguably caused by the northward migration of the forebulge, following the onset of the NAFB.
Our data show that the Jura Mountains experienced relatively minor subsidence during the Paleogene. The Tabular Jura region started to exhume in early-middle Miocene times («20-15 Ma), whereas exhumation in the Jura FTB likely started in the late Miocene («10-5 Ma). This shows an out-of-sequence migration of the deformation in north-eastern Switzerland. As a consequence, it is expected that the deformational trend continued toward the SMB at around 5 Ma.
The exhumation history of the Jura Mountains suggests that the Tabular Jura area, along with its underlying Black Forest Massif, and the Jura FTB should be considered as a potential source of sediments that have fed the SMB since the early-middle Miocene.
The sedimentary overburden that has been removed from the Jura Mountains during the Miocene is about 1 km for the Tabular Jura and 500 m for the Jura FTB, which is significantly lower than some of the traditionally accepted estimates.
Although this work does not represent the first quantitative attempt to determine the timing of deformation and exhumation of the Jura Mountains and the SMB, it is the first providing a time framework for a regional out-of-sequence deformational Miocene trend. In northern Switzerland, the Black Forest Massif is possibly acting as a frontal buttress that hampers forward propagation.
This trend might suggest that tectonic factors are above climate-controlled factors when it comes to explaining the erosional exhumation of the region. It appears that major thrusts operating at depth (e.g., Mandach Fault) play a major role in the uplift and exhumation of the area. Our thermal models suggest that the Jura mountains, although very slowly, are still experiencing uplift and exhumation, as corroborated by earthquake activity.
Supplementary Materials: The following are available online at https://www.mdpi.com/2076-326 3/11/1/10/s1, Table S1: Detailed AFT and LA-ICP-MS data. Funding: This pilot thermochronological project was part of the major UNCONGEO Project ( https://uncongeo.geoenergy.ch/), run by the University of Geneva (GE-RGBA group) and funded by the Swiss Federal Office of Energy (SFOE), the Federal Office of Topography (Swisstopo), Nagra (National Cooperative for the Disposal of Radioactive Waste) and the Cantons of Geneva and Vaud.