Structural organization of the Lorraine coal basin and
formation of the Alsting thrust fold

Metzger Mombo Mouketo, Yves Géraud, Marc Diraison, Allouti Salim, Alain

Izart, Khalid Essa, Claire Bossennec, Fady Nassif

► To cite this version:

Metzger Mombo Mouketo, Yves Géraud, Marc Diraison, Allouti Salim, Alain Izart, et al. Structural organization of the Lorraine coal basin and formation of the Alsting thrust fold. Bulletin de la Société Géologique de France, 2025, pp.1-51. 10.1051/bsgf/2025028. hal-05355473

HAL Id: hal-05355473

https://hal.univ-lorraine.fr/hal-05355473v1

Submitted on 8 Nov 2025

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# Structural organization of the Lorraine coal basin and formation of the Alsting thrust fold

1 *Metzger Mombo Mouketo¹, Yves Géraud¹, Marc Diraison¹, Salim Allouti¹, Alain Izart¹,

2 Khalid Essa²,¹, Claire Bossennec³, Fady Nassif⁴,

3 1: Université de Lorraine, CNRS, Georessources, F-54000 Nancy, France

4 2: Geophysics Department, Faculty of Science, Cairo University, Giza, P.O.12613, Egypt

5 3: Université de Lille, Section 36, Terre solide, Géodynamique des enveloppes supérieures

6 4: La Française de l'Energie (FDE), France

7 Author address: metzger.mombo-mouketo@univ-lorraine.fr

## Résumé

11 Le Bassin Houiller Lorrain (BHL), rempli de formations détritiques continentales d'âge
12 Carbonifère supérieur-Permien, s'est développé le long de la Zone de failles de Metz-Hunsrück.

13 Malgré de nombreuses études structurales, la structure de son socle qui contrôle les variations
14 des épaisseurs des séries sédimentaires et la formation du pli d'Alsting ont très peu été
15 investiguées. Dans cette étude, l'analyse des données gravimétriques a permis de cartographier
16 la zone de faille de Metz-Hunsrück, et plus globalement la géométrie du toit du socle sous le
17 bassin. L'analyse des lignes sismiques 2D et des données de puits a permis de contraindre la
18 structure et la formation du pli d'Alsting.

19 La carte du toit du socle met en évidence une structuration en hauts de socle (-1,5 km) et des
20 zones d'approfondissement de socle (-6,5 km) orientés NE-SW, NNE-SSW à N-S et NW-SE.

21 Cette structuration explique les variations spatiales des épaisseurs des séries sédimentaires en
22 place. La première dérivée verticale de l'anomalie de Bouger montre que la zone de faille de
23 Metz-Hunsrück est continue et limite les bassins houillers lorrain et sarrois.
Par ailleurs, les interprétations sismiques montrent que le pli d'Alsting est un pli-faille dont la formation et l'érosion post-compression se sont produites pendant le Stéphanien. Après cette déformation, la subsidence et de dépôt ont repris à la fin du Stéphanien.

Cette étude met en évidence une histoire géologique Stéphanienne différente du bassin Lorrain par rapport aux autres bassins du même âge due à sa position structurale.

## 29 Abstract

The Lorraine Coal Basin (LCB), filled with continental clastic formations of the Upper Carboniferous-Permian age, developed along the Metz-Hunsrück-Fault-Zone (MHFZ). Despite the structural studies, the structure of the basement which control the total sedimentary thickness variations, and the Alsting fold structure and formation remains poorly constrained.

In this study, the analysis of gravity data has allowed to map the MHFZ and more regionally the top basement structures beneath the basin. The analysis of 2D seismic lines and well data analysis has allowed to constrain the structure and formation of the Alsting fold.

The top basement map highlights the presence of highs (-1,5 km) and deeps (-6,5 km) trending NE-SW, NNE-SSW to N-S and NW-SE. This structuration explains the global sedimentary thickness variation of the sedimentary series in place. The first vertical derivative of the Bouger anomaly suggests that the MHFZ is continuous throughout the LCB and the SNCB.

Furthermore, seismic interpretations show that the Alsting fold is a thrust fold whose formation and post-compression erosion occurred during the Stephanian. After this deformation phase, subsidence and deposition restarted during the late Stephanian. This study highlights a different Stephanian geological history of the BHL compared with other basins of the same age due to its structural position.
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**Keywords**

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Lorraine Coal Basin, Basement and basin structure, Stephanian compression, Metz-Hunsrück-Fault-Zone, Thickness variations, Alsting thrust-fold formation.

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**1. Introduction**

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The Westphalian coal seams of the Lorraine Coal Basin (LCB) and its prolongation in Germany known as the Saar-Nahe Coal Basin (SNCB) (Fig. 1) have been long exploited while less economical attention was paid to their methane content. Since 2015, this methane has been explored by La Française de l'Energie company (FDE). This momentum led to the creation of the REGALOR project (REssources GAzières de LORraine) that aims in part to re-evaluate the structural organization of the basin for a better characterization of this resources. After the review of the literature in the basin, the structure Metz-Hunsrück-Fault-Zone (MHFZ) and that of the basement beneath the sedimentary cover as they are still badly constrained. For that, the first vertical derivative and the top basement map are constructed from the Bouguer to highlight the geometry of both structures and understand their relationship with the total thickness variation in the basin. Furthermore, within the FDE exploration permit (located in the north-eastern part of the basin), most of the previous structural studies focused on the Merlebach (MTF), the Saarbrucken (STF) and the Pont-à-Mousson (PaMTF) thrust folds (Pruvost, 1934; Donsimoni, 1981; Pryvalov et al., 2015; Beccabetto et al., 2019; Hemelsdaël et al., 2023) while the Alsting fold (ATF) (Fig. 2a) did not received much attention. Since it is a target for the company, deciphering its structure and its formation is useful for its exploration but also to understand the full picture of the deformation evolution in the LCB. A set of 2D seismic lines (Fig. 2a) and well data provided by la FDE are used for this purpose.
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## 2. Geological context

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### 2.1. The LCB-SNCB in the framework of the Variscan belt

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The LCB and the SNCB form a north-east to north-north-east trending Upper Carboniferous-Permian basin that extends by 300 km long and 80 km width (Fig. 1), with almost 6-7 km of preserved strata (Donsimoni, 1981). The basin developed on the Mid German Crystalline High (MGCH) during the late variscan period due to the activity of the Metz-Hunsrück-Fault-Zone (MHFZ), which limits the basin in the north (Pruvost, 1934; Donsimoni, 1981; Anderle, 1986; Henk, 1993; Korsch and Schäfer, 1995; Schäfer, 2011). The basin is limited by other major variscan structures (Fig.1), the La Marne fault (MaF) in the west, and the saxothuringian limit in the south (Donsimoni, 1981; Franke, 2014). The basin's development is linked to the orogenic and post-orogenic deformation evolution of the rhenohercynian and the MGCH (Donsimoni, 1981; Anderle, 1986; Henk, 1993; Korsch and Schäfer, 1995; Hemelsdaël et al., 2023).

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The orogenic period was marked by the convergence between the rhenohercynian unit and the MGCH during Frasnian and the Upper Carboniferous (Oncken, 1998). This convergence led to the folding and thrusting of the Devonian-Lower carboniferous marine strata deposited on the rhenohercynian unit were. From Namurian-Westphalian, the deformation propagation of the variscan front toward the north initiated the development of foreland paralic coal basins such as the Ruhr and the Namur (Fig.1) whereas the LCB and SNCB and other limnic coal basins developed on the MGCH (Pruvost, 1934; Alpern et al., 1969; Zimmerly, 1976; Donsimoni, 1981; Schäfer, 1989). Yet, from the Westphalian, the stress regime under which the LCB and SNCB developed is still debated. The geodynamic models proposed by Arthaud and Matte (1977) and Burg et al. (1994) which suggests a syn-orogenic extension/transtensional regime during Westphalian and a post-orogenic extension during Stephanian-Permian as largely been used to explain the basin's development (Donsimoni, 1981; Korsch and Schäfer, 1995;
93 Privalov et al., 2015; Henk, 1993) and that of several other coal basins (Faure, 1995; Henk, 1993; Donsimoni, 1981; Korsch and Schäfer, 1995; Djarar et al., 1996; Allemand et al., 1997; Averbuch et Piromallo, 2012; McCann et al., 2006). However, other authors (Anderle, 1986; Kroner et al., 2008; Corsini and Rolland, 2009; Kroner and Romer, 2013; Stephan et al., 2016) argued for a compressional/transpressional regime during the Namurian-Westphalian in the rhenohercynian and saxothurigian units. Anderle (1986) links the LCB and SNCB initiation to this compressional/transpressional regime.

100 After this compressive setting, the Late Carboniferous-Permian period was governed by extension and magmatism (Faure, 1995). In the SNCB, the volcanism is Permian and dated close to 290 Ma (Lippolt and Hess, 1989), while there is no absolute dating in the LCB (Donsimoni, 1981). During Triassic, a continental and restricted marine setting developed (Guillocheau et al., 2000) over the rhenohercynian domain and the MGCH that led to the shallow burial of the LCB and SNCB Upper Carboniferous-Permian strata. During the Jurassic and the Lower Cretaceous, the LCB, the SNCB, and the southern part of the Hunsrück-Taunus formation were deeply buried under the Mesozoic formations (Guillocheau et al., 2000; Prijac et al., 2000; Le Solleuz et al., 2004). Later during Cretaceous, the rhenohercynian domain was uplifted and a part of the SNCB underwent an erosion (Anderle, 1986; Hertle and Littke, 2000). This erosion made a part of the Upper Carboniferous formations of the SNCB outcrop (Fig.2a).

## 2.2. Existing tectono-sedimentary models of the LCB and SNCB

### 2.2.1. The Lorraine Coal Basin (LCB)

113 Different structural models have been proposed for the LCB. Pruvost (1934) was a pioneer scientist that discussed the global structural evolution of the basin. Donsimoni (1981) was the first to propose that the basin developed due to the reactivation of the MHFZ as a normal fault. He summarised its tectono-sedimentary evolution into four major stages: (1) the deposition of
117 the Namurian-Westphalian D, (2) a weakly folding phase during Late Westphalian D, (3) a
118 renew of the subsidence and deposition during Stephanian-Permian, (4) and finally the major
119 folding and thrusting phase during Mid-Permian. Micro-structural data measured on thrusts and
120 on strike-slip faults in galleries suggest that the compression was oriented NW-SE (Blès and
121 Lozes, 1980; Donsimoni, 1981). This Permian shortening phase led to the current organisation
122 of the fold and synclines (Fig. 2b) according to the author.

123 Pryvalov et al. (2015) interpreted the LCB and the SNCB as a large pull-apart basin with a local
124 extension-compression due to the basement-block rotations. The author interpretation is based
125 on the observation of the cleat (fractures in coal seams) geometry through the X-ray tomography
126 without any observations at the basin scale.

127 More recently, Beccaletto et al. (2019) and Hemelsdaël et al. (2023) show that LCB developed
128 as a compressive basin along the Metz thrust (a NW-dipping thrust) during the Namurian-
129 Westphalian. In addition, their seismic interpretations highlighted Westphalian C and D growth
130 strata involved in the PaMTF that led to infer that age of the deformation in the basin..
131 Furthermore, the authors highlighted syn-sedimentary normal faults that control the Stephanian
132 strata deposition in the south-western part of the LCB (Fig.2a). At the basin scale, the author
133 interpret these faults as the consequence of the post-orogenic extension accommodated by the
134 Hunsrück fault. This model suggest that the Metz-Fault and the Hunsrück Fault are two
135 different faults.

2.2.2. The Saar Nahe Coal Basin (SNCB)

136 In the SNCB, three different structural models were proposed based on different interpretations
137 of the MHFZ imaged by the DEKORP 1C-9N seismic line. Anderle (1986) interpreted the
138 SNCB as a compressive basin from the Namurian until the Late Westphalian and which
139 switched into an extensional one during Late Carboniferous due to the collapse of the variscan
140 orogeny. Anderle (1986) suggested a Late Carboniferous compression for the Saarbrücken
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142 thrust-fold formation while Engel (1985) suggested a Stephanian-Permian compression. Before
143 the well-known paper of Korsch and Schäfer (1995), the Saarbrucken thrust fold has been
144 interpreted as a positive flower structure linked to the strike-slip motion along the MHFZ
145 (Drozdzewski and Juch, 1992; Juch et al., 1994). Korsch and Schäfer (1995) interpreted the
146 LCB and the SNCB as a transtensional pull-apart based on the : (1) the interpretation of the
147 MHFZ as a steep fault, (2) the north-eastward depocenter migration from the LCB to the SCB
148 deduced from thickness maps from well data and (3) the subsidence curve which is like those
149 of strike-slip basins.

150 Henk (1993) on the contrary, interpreted the MHFZ as a detachment fault. The author proposed
151 that the SNCB developed as a compressive basin until Westphalian B and which became an
152 extensional basin due to the E-W extension from Westphalian C. In this model, the extensional
153 reactivation of the MHFZ leads to the collapse and segmentation of the MGCH basement into
154 sub-blocs separated by first order NW-SE right-lateral transtensional faults (Fig. 2a). These
155 NW-SE first-order faults created sub-basins separating the LCB with the SNCB. This collapse
156 led to the formation of the Saarbrucken thrust fold according to Henk (1993). Such first order
157 transfer faults have never been clearly observed on seismic data. However, the second and third
158 order NW-SE, and E-W strike-slip faults (Fig. 2a) segmenting the LCB-SNCB into small horsts
159 and grabens have been proved (Engel, 1985; Stollhofen, 1998; Juch et al., 1994; Becker and
160 Schäfer, 2020, 2021).

## 2.3. Lithostratigraphy of the LCB

161 Two Upper Carboniferous stratigraphic sub-stages (Fig. 3) have been defined in the LCB and
162 the SNCB based on paleontological studies (Bertrand, 1928; Pruvost, 1934; Laveine, 1974;
163 Kelch and Reible, 1976), palynology (Alpern et al., 1969) and on of well-known tonstein layers
164 (Termier, 1923; Pruvost, 1934; Merry, 1967; Lippolt and Hess, 1989; Burger et al., 1997;
165 Koniger et al., 2002). The Namurian-Westphalian, the oldest interval, consists of almost 4 km
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167 of finning upward sequences of conglomerates, sandstones with intercalated
168 siltstones/claystones, and multiple coal seams. These sequences deposited in alluvial, braided,
169 meandering fluvial, floodplain or swamps, and lacustrine environments (Donsimoni, 1981;
170 Schäfer, 1989; Izart et al., 2005). The petrographic components of the Westphalian sandstones
171 and conglomerates suggest that the Rhenohercynian metamorphic and sedimentary massif was
172 the principal sediment source (Pruvost, 1934; Schäfer, 2011). The Westphalian was subdivided
173 into Westphalian A, B, C, and D sub-stages based on plant distribution. These continental sub-
174 stages correspond respectively to the Langsettian, Duckmantian, Bolsovian, and Asturian
175 (Aretz et al., 2020). Izart et al. (2025) have just published the first absolute dates in the BHL.
176 These confirmed the stratigraphic age of tonstein T600 (Duckmantian-Bolsovian boundary),
177 from tonsteins T10 to the top of the Asturian. The continental nomenclature will be preferred
178 in this study to ensure consistency between well data lithostratigraphy and seismic horizon
179 interpretation.

180 The second sub-stage recognized is the Stephanian, whose basis is represented by the Holz
181 conglomerate formation (Fig. 3), which is often discordant with the underlying Westphalian. In
182 the LCB, only the Early Stephanian is known (Alpern et al., 1969) while the entire Stephanian
183 is recognized in the SNCB (Schäfer, 2011). Izart et al. (2025) dated the other tuffs and
184 constrained the hiatus below the Holz conglomerate, which corresponds to 2 Ma. This hiatus
185 corresponds to the Lower and Middle Cantabrian stage (Izart et al., 2025) and is due to the post-
186 folding erosion (Pruvost, 1934; Donsimoni, 1981; Hemelsdaël et al., 2023). Absolute dates
187 are also available for the SNCB from several studies (Burger et al., 1997; Königer et al., 2002;
188 Königer and Lorenz, 2002; Menning and Bachtadse, 2012; Voigt et al., 2022). According to
189 Schafer (1989), the richness in feldspars and the change of the paleo-current sense suggest that
190 the sediment was supplied by the granitic massifs in the south.
Both formations are overlain by the Lower Permian continental red sediments, which are heterogeneously recognised in both basins (Schäfer, 2011). The two sub-stages (Lower Rotliegend equivalent to Autunian and the Upper Rotliegend) are recognised in the SNCB while only the Saxonian facies, equivalent to a part of the Upper Rotliegend has been recognised in the LCB (Donsimoni, 1981). In the LCB, this Saxonian facies can easily reach 700 m of thickness (Donsimoni, 1981) and is composed of continental red conglomerates, sandstones, and claystone, deposited in alluvial, fluvial, and lacustrine environments (Donsimoni, 1981; Schäfer, 2011). Furthermore, several magmatic intrusions and sills (basaltic, andesitic, and rhyolitic intrusions and sills) affected SLB during the Early Permian (Lippolt and Hess, 1989). In the LCB, the volcanic bodies have been mapped using seismic, gravity and well data, but have never been dated (Donsimoni, 1981; Hemelsdaël et al., 2023).

## 3. Dataset

Dataset used in this study comprises a network of 2D seismic lines (Fig. 2a), mining and petroleum wells (Fig. 4a), and gravity data which are detailed in the following sections.

### 3.1. Well data

Fig. 4a presents the location of all the wells used in this study. Most of the wells named SJ prefix have been drilled by the HBL (Houillère du Bassin Lorrain) company during the mining explorations to characterize the coal seams. They possess a very detailed description of the facies, the different tuffs layers (tonsteins), and the palynology of the different units crossed, allowing to identify the different Carboniferous sub-stages limits. These wells can be freely downloaded (infoterre). The rest of the wells were drilled during the exploration of hydrocarbons and possess logging data, and the different stratigraphic stages and sub-stages limits were determined by palynology as well.
## 3.2. Gravity data

The Complete Bouguer Anomaly data (CBA) used covers the LCB, the SNCB, and their surrounding basement units. The data is part of the work of the AlpArray Gravity Research Group (AAGRG) (Zahorec et al., 2021). The CBA was corrected using an average density of 2,670 kg.m⁻³, and the terrain corrections were made with different DEM (Digital Elevation Model) of different resolutions, ranging 5 m to 30 m (see Zahorec et al., 2021 for more details).

To map the geometry of the MHF, the First Vertical Derivative (FVD) of the residual Bouguer anomalies was computed to enhance the anomalies for better interpretation (Fig. 5). The map top basement map (Fig. 6) is generated through the application of the Source Parameter Imaging Method (Thurston and Smith, 1997; Smith et al., 1998; Essa et al., 2022). Furthermore, a spectral analysis was applied on the Bouguer anomaly. This allows to identify the depth of the different gravity anomalies and to separate the regional from the residual anomalies (Spector and Grant, 1970; Essa et al., 2018; Mazur et al., 2020; Ganguli et al., 2020).

## 3.3. Seismic-to-well tie

The eight seismic lines presented in this study are located in the north-east part of the LCB (Fig. 2a) and were provided by “Française de l’Energie” (FDE) company. They comprise six post-stacked migrated seismic lines (SAR5, SAR7, SAR16, SAR17, SAR18, and SAR20) acquired in 1989 and two vintage seismic lines (RE01 and RE04) acquired in 1958. Amplitude corrections (AGC: Amplitude Gain Correction), DMO (Dip-Move-Out) correction and post-stack migration were applied to the SAR lines by the FDE. The vintage lines were depth-migrated using linear velocities laws. No further information is available about this time-to-depth conversion. Their quality is poorer compared to the SAR lines. The Seismigraphix open-source software was used to display the 6 SEG-Y seismic lines in order to obtain a high-resolution images and their interpretation were done in Adobe Illustrator 2019.
The seismic-to-well-tie method does not rely on check-shot since they are not available on the wells located in our study area. However, the sonic log was used to convert the top of each Carboniferous sequence crossed by the Vaxy (Va), Morhange (Mo-1) and Germisay (L.Ge-1) well into time by using the sonic velocities of conglomerate, sandstones, claystones and coals, and the percentages of facies in each carboniferous sequence (Fig. 4b). This time was compared with the interpreted limit of each formation in the seismic lines. The intersections between these seismic lines allowed us to know the time of each formation in all the seismic sections.

# 4. Results and interpretations

## 4.1. Basement structuration

### 4.1.1. The structure of the gravity anomalies

Fig. 5 presents the interpretations of the first vertical derivative which shows that the rhenohercynian unit, the LCB and the SNCB, and the Vosges-Black domains are structured by an alternation between NE-SW trending gravity highs (warm colours) and gravity deeps (blue areas) (Fig. 5) consistent with the orientation of the major Variscan basement lineaments in the area (Edel and Schulmann, 2009). The most interesting gravity highs are the H1, H1' and the H2 in the rhenohercynian area (Fig. 5). In detail, the H1 is a continuous lineament from the SNCB (where the MHFZ crops out) until the Metz city in the LCB (Fig. 5). Then it becomes discontinuous and less straight from the Metz to the South-Western part of the LCB where it is buried under the Mesozoic-Triassic and the Stephanian-Permian strata. In addition, the MHFZ shows strike changes from the SNCB until the LCB. The significance of all these anomalies is discussed further.

### 4.1.2. The basement top structure

The basement here are the MGCH and the Devonian-Mississippian metasedimentary formations beneath the LCB and the SNCB. Unlike the well data, the overall map of the
basement top (Fig. 6) allows to have a continuous picture of the global thickness variations of the sedimentary cover. A comparative analysis was conducted using this map and the wells which reach the basement. For the Gironville (Gi) well, the top basement is at 5.6 km of depth, and our estimation from gravimetric data predicts 5.6 km of depth, showcasing a good agreement. However, for the Saarbrücken (Sa-1) well in the SNCB, the recorded depth of the basement top is around 5.6 km, which does not fit with the corresponding computed values around 4.6 km.

Nevertheless, this map highlights a complex geometry of the basement top with the presence of highs (1.5 – 3 km) and deeps (> 4 km) of different sizes, geometries and orientations.

Regarding the deeps, the NE-SW and the NNW-SSE are the dominant structures. The NE-SW deeps align with the major synclines (Landroff, Pirmasens and the Sarreguemines) in both basins except in the SNCB where map shows a large basement high highlighted by the violet dash-line in the Nahe-syncline (Fig. 6). The deeps length varies between 10 and 50 km and their width between 5 and 20 km. Some of the NW-SE deeps align with the NW-SE faults (Fig.6). Their length varies between 10 and 30 km and their width between 5 and 10 km (Fig. 6).

Regarding the deeps, the deep located in the Nahe-syncline is the largest with 130 km of length and a width varies from 20 to 40 km (Fig. 6). The other deeps are located at the LCB south basin borders, below the city of Nancy, around the Courcelles (Cou) well, and near the MAF fault. The significance of all these structures is discussed further.

## 4.2. Basin structuration

### 4.2.1. Sedimentary thickness from wells

Fig. 7 gives important insights on the thickness variations, particularly for the Triassic-Mesozoic, the Permian, and the Stephanian sequences which are entirely crossed by many wells. The first striking observation is the less important thickness of the Triassic-Mesozoic sequence toward the north-east of the LCB along all the well profiles. The second interesting
observation in the north-eastern part of the LCB is that the Permian and Stephanian sequences are thinner to absent at the fold hinge but thicker in the Landroff and Sarreguemines synclines.

The Permian sequence thickness at the anticline crest is about 50 to 150 m while it is two or three times thicker (300 - 400 m) in syncline position. Likewise, the Stephanian sequence is thinner (100-200 m) to be absent in the anticline crest (SJ234, LRT-1, SUY-1, SJ64, SJ424, SJ680, and SJ393) while it is thicker (500 m -1.2 km) in the syncline. There is an exception for some wells (SJ239; Mo-1; SJ386; SJ244; SJ681; and the SJ385) located at anticline crests and which show thicker Permian and Stephanian formations. Nevertheless, all these observations suggest a close relationship between the folds and the spatial thickness variations of the Stephanian-Permian sequences.

In the south-western apart of the LCB, the wells highlight the same tendency but with a thicker Stephanian and Permian (1-2 km) compared to the thickness range observed in the north-eastern part. The thicker Permian is encountered on Germisay well (L.Ge-1), Chevraumont (Chv), Commercy (Co) wells. In the SNCB, the Land-1 and AD-1 wells, located in the Pirmasens and the southern limit of the LCB-SNCB basin show a similar range of thickness. For the Westphalian D, C, and B sequences, is it very difficult to identify a relationship with the anticline and syncline since their thickness are not entirely crossed by the different wells. The last interesting characteristic highlighted by these wells is the presence of the basement at shallow depth (800 m -1.6 km) in the northern limit of the LCB.

### 4.2.2. Structure of the Alsting and the Merlebach anticlines

#### 4.2.2.1. Seismic stratigraphy

Four stratigraphic sequences have been depicted on seismic lines (Fig. 8, 9, and 10) based on the time-depth presented on Fig. 4b: they are the Triassic-Mesozoic, the Permian, the Early Stephanian, the Westphalian and the basement. The top basement located between 2.6-3.1 s (twt) is composed of continuous reflections in the uppermost part while the lower part is badly
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imaged and represented by the multiples of the upper part reflections (Fig. 8, 9, and 10). The
SAR07 line (Fig. 10a) highlights the shallowing of its reflections, from 3,1s in the north-west
and reaching 2.6 s (twt) toward the south-east.

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The Westphalian is divided into the Westphalian D and the Undifferentiated Westphalian
C/B/A separated by the Top Westphalian C limit (TWC) (Fig. 8, 9, and 10). Both sub-sequences
are composed of folded and thrusted reflections. These reflections are affected by erosion in the
anticline crest. In detail, they consist of an alternation between low and high-amplitude and
continuous reflections, which correspond to an alternation between coal seams and
conglomerates and sandstones (Izart et al., 2005). The Early Stephanian sequence rest
conformably on the underlying Westphalian strata, implying a non-interrupted sedimentation.
This allows to define the CSB as the Conformable Stephanian Basis (Fig. 8, 9, and 10).
Moreover, the Intra-Stephanian Unconformity (ISU) is defined within the Early Stephanian
formations, separating a folded Stephanian sub-sequence with a non-folded upper sub-
sequence. The upper sub-sequence is composed of reflections that fill the syncline and thin
toward the hinge while the lower sub-sequence reflections are folded and thrusted.

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Under the Mesozoic-Triassic formations, the Permian sequence is composed of horizontal and non-folded reflections which fill the piggyback and frontal synclines. The Permian Basis (PB) is often an irregular surface and sometimes truncates the underlying Stephanian-Westphalian, showing an erosion before the Permian deposition. This is the case at the Merlebach hinge (Fig. 11).

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The Triassic-Mesozoic sequence is composed of an alternation between low and high-amplitude continuous reflections (Fig. 8, 9, and 10). The Triassic-Mesozoic Basis (TMB) can be flat or irregular, and all the reflections drape the underlying Permian-Pennsylvanian strata. Furthermore, these reflections are affected by normal faults and gently folded at the location of the thrust fold hinge (Fig. 11).

333

334

335

336
337 **4.2.2.2.The Alsting anticline.**

338 The Alsting anticline is imaged by the SAR 5, 7, 16, 17, and 18 (Fig. 8, 9, and 10b) which are
339 perpendicular to the fold but also by the SAR20 (Fig. 10b) which is parallel to the fold strike.

340 The SAR 5, 7, 16, 17, and 18 show that the Westphalian sequences (Westphalian D/C/B/A) are
341 folded and thrusted by a NW-dipping fault which soles out around within the Westphalian
342 sequence at 2.5 s (twt). Furthermore, there is no thickening of the Westphalian strata along the
343 thrust, neither any visible preserved normal throw. In the piggyback syncline (the Landroff
344 syncline), the ISU separates a lower sub-sequence made up of folded strata with an upper sub-
345 sequence made up of horizontal strata. However, on SAR20, the transition zone between the
346 Alsting and the Morhange shows these Stephanian reflections overlaying the ISU with a fan-
347 shape geometry.

348 **4.2.2.3. The Merlebach anticline.**

349 The Merlebach anticline is imaged by the RE 01crossline and the RE 04 strike line (Fig. 11a
350 and b). The RE 01 (Fig. 11a) highlight the anticline as an open thrust fold, with the thrust
351 dipping toward the NW and affecting both the Westphalian sequence and the lower Stephanian
352 sub-sequence under the ISU. Yet, the back limb of the thrust fold is very difficult to interpret
353 due to the low quality of the line. More importantly, the line shows the strong bending of the
354 Westphalian strata in the Landroff syncline and a thick (2 km) Lower Stephanian sequence over
355 the ISU. In the Merlebach back limb (Fig. 11b), the RE 04 line highlights the presence of NW-
356 SE normal faults that develop in the Lower Stephanian under the ISU.

357 **5. Discussion**

358 **5.1. The structure of the Metz-Hunsrück Fault Zone (MHFZ)**

359 This part discusses the structural and geological significance of the different gravity anomalies
360 highlighted on Fig. 5. If we compare the position of the gravity highs and deeps in the
361 rhenohercynian domain with its cross-section from Oncken et al. (1999), it appears that the
362 gravity deeps correspond respectively to the folded and thrust Devonian metasedimentary of
363 the Hunsrück Nappe and the Mosel synclinoriums. Regarding the gravity highs, the H1
364 corresponds to the MHFZ, the H1'might correspond to a secondary fault zone that branches to
365 the MHFZ, and the H2 is probably the Boppard thrust system zone and not the Hunsruck suture
366 as proposed by Hemelsdaël et al. (2023). The gravity highs might then be interpreted as the
367 signature of the pre-Devonian basement rocks that are involved in these thrusts' zones.

368 Furthermore, Fig. 5 highlights almost a general strike change of theses highs and deeps toward
369 the south-west, where they almost become E-W tending anomalies. These data show that the
370 MHFZ is a complex fault zone than previously thought.

371 Within the LCB and the SNCB, Edel and Schulmann (2009) interpreted the gravity deeps in
372 the LCB and SNCB as the signature of a crystalline ridge (the MGCH granite/metagranite) and
373 the gravity high in the Sarreguemines syncline as the Morhange thrust zone and the Teplà-
374 suture zone. Finally, the gravity highs and deeps are linked to the basement structures, and the
375 sedimentary cover effect seems to be insignificant.

377 **5.2. Tectonic structures and sediment thickness**

378 **5.2.1. The basement highs and deeps**

379 The depth derived with the basement top map fit very well with the depth encountered on
380 Gironville well and Land-1 well but not for some areas or wells as it is the case of the Sa-1
381 well, and the depth estimated in the Nahe syncline. Therefore, the significance of these
382 basement highs and deeps must be discussed.

383 The first interesting feature to discuss is the basement high which correspond to the Nahe
384 syncline and its prolongation in the LCB. This high suggests a sedimentary thickness less than
385 4 km while Korsch and Schäfer (1995) and Schäfer (2011) cross-sections suggest more than 7
386 km. Yet, the Saint-Wendel (Stwe-1) and the Monzingen (Monz) wells drilled on this basement
387 high only cross the Permian strata until 2 km (Fig. 3, Schafer, 2011). Similarly to the SNCB,
388 the SJ206, and the SJ203 in the LCB cross a thicker Permian (625 m) and reaches the
389 Stephanian at 1.2 km (Fig. 6). All these well data therefore cannot help to be sure of the depth
390 of the top basement predicted by our algorithm nor that suggested by the previous authors.
391 However, the cross-section of Hannover (1979) on the Figure 3 from Izart et al. (2016) supports
392 the presence of the Devonian formations belonging to the rhenohercynian unit between 1.5 and
393 3 km under a thick Permian and a thin Stephanian sequence, fitting with our basement high. In
394 this case, the southern limit of the high might correspond to the Metz-Taunus Fault sensu
395 Hannover (1979). This shows ha the MHF zone is a very complex fault zone with several fault
396 secondary faults connecting to one another. The other explanation of this basement high could
397 be linked to the presence of several volcanic bodies in the Nahe syncline (Schäfer, 2011). These
398 volcanic bodies are elongated and are present almost everywhere in the Permian sequence of
399 the Nahe syncline. As the algorithm assumes that the long wavelength anomalies correspond to
400 the basement anomalies, the algorithm could have confused their anomalies with the signature
401 of the basement. The other interesting basement high is located at the PaMTF. This might
402 correspond to the basement involved in the PaMTF as shown by Hemelsdaël et al. (2023).
403 Regarding the basement deeps, The Landstühl well (Land-1) located in the circular shape deep
404 crosses the Permian basis at 3 km (Becker and Schäfer, 2020; 2021), and the seismic line A
405 (Schäfer, 2011) predict 3 km of Westphalian-Stephanian under this Permian basis. These two
406 observations predict a 6 km depocenter, matching well with the map. Becker and Schäfer (2020)
407 suggest the Permian sequence is made up of half-graben bounded by NW-SE transfer faults.
408 The geometry and the orientation of the deeps (Fig.6) may indicate that they are bounded by
409 NW-SE faults. In this case, such faults might affect the basement top as well. The other
410 basement deep which seems to be controlled by the NW-SE fault is located above the
Saarbrücken city. In the north-eastern part of the LCB, the elongated NE-SW basement deep in the north-eastern part of the LCB aligned with the Landroff syncline. Within this deep, the seismic line RE01 highlights a Stephanian depocenter with the basis located at almost 4 km, overlaying a thick Westphalian sequence whose basis is probably deeper than 6 km. The depth and the structure observed on this seismic line agrees with the map.

In the southwestern part of the LCB, the case of the Gironville-Francheville deep, located between the CoF and the MoF, correspond to a thick (3s-twt thick) Westphalian syncline overlain by the Stephanian sequence controlled by the ToF (Fig. 6, Hemelsdaël et al., 2023).

Furthermore, this Figure 6 shows the basement top at 3.3 s (twt) fitting with the depth predicted by the map. According to the interpretation on Figure 7 from Hemelsdaël et al. (2023), the Meligny and Chevraumont deeps correspond to the Gironville-Franchville depocenter. Our map show that both deeps seem to be laterally offset, probably indicating a sinistral displacement on the CoF. Meligny well (Mny) does not reach the Westphalian but shows a thick Triassic-Mesozoic until 1.75 km. The Chv well cross the Stephanian until 2.5 km. Hemelsdaël et al. (2023) interpreted the basement top at 2.5 s (twt) suggesting a less important global thickness than the 5 km predicted by our map. Yet, our map and the seismic lines in Hemelsdaël et al. (2023) both highlight the basement structuration. This structuration can be related to the folding of the basement when the basin underwent compression or simply represents the inherited basement structuration. The L.Ge-1 well, located on the border of this depocenter, encounters 1.4 km of Stephanian-permian sequence and 1.3 km of Permian. Our map predicts a thicker sedimentary cover (around 6 km), which can suggest that there is a 3 km thickness of the Stephanian-Westphalian formations before reaching the basement top. Furthermore, by making the seismic-to-well tie on the Toul 12 with this well (Fig. 4b), it appears that the Permian basis is likely located at 2s, and the Stephanian basis at 3.2 s, which is also in agreement with the thickness ranges predicted by the map.
436

### 5.2.2. The fold hinge area, the piggyback and the growth syncline

437

438

439

440

441

442

443

444

445

446

447

448

449

450

451

452

453

454

455

456

457

458

459

460

The different tectono-sedimentary evolution recorded at the fold hinge and in the synclines allow to explain some of the thickness variations trends observed for the Stephanian-Permian formations. The low thickness observed at the fold hinge areas is explained by the post-compressional erosion of the folded sub-sequence under the ISU and to the low thickness or the non-deposition of the upper sub-sequence of drape strata overlaying the ISU. On the contrary, the high thickness of the Early Stephanian observed in the piggyback syncline is due to the preservation of both sub-sequences. Pruvost (1934) map highlights that the erosion at the Westphalian-Stephanian limit is more important around the Saarbrucken thrust fold as the Holz-conglomerate rests on the C and B. On the SAR 5 (Fig. 9b), the ISU rests on the Westphalian D and C while it rests only on the Westphalian D in the other seismic lines, proving different local erosion rates under the Holz-conglomerate as highlighted by Pruvost (1934).

The low Permian thickness observed at the hinge area is due to post-depositional erosion. The low Permian thickness observed at the hinge area is due to the Permian and Triassic erosion. Furthermore, the geometry characteristic of the Mo-1 syncline revealed by the SAR20 (Fig. 11b) and the lateral evolution of the depth of the Stephanian basis reflection from the Alsting to the Morhange thrust folds (Fig. 12) allows to conclude that the Morhange syncline is a relay growth syncline. The fan-shape geometry of the Early Stephanian reflections explains the high thickness (1.2 km) observed on the Mo-1 well. At the Morhange hinge (Fig. 12), the low thickness observed on Va well is explained by the thinning of the Stephanian (from 0.5s in the Landroff syncline to 0.2s at the Morhange hinge) as interpreted by Hemelsdaël et al. (2023). The same fan-geometry is observed for the thick (2km) Stephanian sequence on the RE 01 (Fig.11b). Therefore, another explanation of the high thickness of the Stephanian sequence in the syncline area and their low thickness at the hinge area might be due to the growth nature of these strata.
For the Triassic-Mesozoic sequence, the thickness variations are linked to the post-variscan history. The less important thickness of these formations in the north-east of the LCB are due to a more important erosion of the Paris basin formations (Blaise et al., 2014; Izart et al., 2016) by using the 1D burial and thermal modelling of the boreholes EST433 (close to Germisay) and the Rn8 (close to Nancy).

### 5.2.3. The NW-SE faults

The role of NW-SE faults on the Permian and Stephanian sequences thickness variations have been largely been described in the LCB and SNCB (Pruvost, 1934; Engel, 1985; Stollhofen, 1998, Donsimoni, 1981, Becker and Schäfer, 2020, 2021; Hemelsdaël et al., 2023). The only seismic lines in our dataset that can image such faults are the SAR20 and the RE04 as they are oriented perpendicular to the fault's orientation. For the Permian sequence, the two lines show that the strata drape the folded and eroded anticline, they are not controlled by any NW-SE faults. Furthermore, some of these NW-SE syn-sedimentary normal faults are visible on the RE04 line (Fig. 11b) in the Lower Stephanian under the ISU.

However, it is difficult to assess the syn-sedimentary activity of the LoF and the DeF only with well data. The SJ239 located between these two faults (Fig. 4a), show a 300 m thick for the Permian formations (Fig. 7). This high thickness might indicates the effect of one of these faults. Yet, the well is in a syncline which can explain a high preservation of the Permian formations. Likewise, even if the SJ244 shows a thicker (120 m) Permian than in the SJ234 (10 m) (Fig. 7), it is difficult to relate this high thickness to the fault activity since the SJ244 is in a relay syncline (Fig. 4a). Moreover, the SJ234 is located at the PaMTF hinge, which underwent an important erosion which can explain the low Permian thickness (10 m). This erosion may explain the absence of the Stephanian formations in this well. Therefore, the presence of such faults and their role in thickness variation is much localised in the LCB.
### 5.3. Tectono-sedimentary evolution of the Alsting thrust-fold.

Considering that there is no thickening of the Westphalian strata along the thrust, any visible preserved normal throw, and considering the geometry of the thrust, the Alsting thrust-fold is interpreted as a fault-propagation fold. The fact that its thrust soles out within the Westphalian sequence (at 2.2s twt, according to our interpretation) may indicate a thin skin-deformation style in this area. The SAR 7 (Fig. 10a) on which the Westphalian-basement interface is better imaged (at 3s) shows no deformation of the basement, supporting our suggestion of a thin-skin deformation style.

Furthermore, as regard to the timing of the Alsting fold, the drape sequence that deposited after the ISU development leads to conclude that the fold was formed during the Early Stephanian. Therefore, a tectono-sedimentary evolution of the Alsting thrust fold is proposed on Figure 13.
After a continuous sedimentation from the Westphalian until the Early Stephanian, the LCB was affected by the Variscan compression leading to the formation of the Alsting thrust fold (Fig. 13a). The Alsting hinge was uplifted to the surface and underwent an important erosion leading to the ISU formation (Fig. 13b). The sediment eroded probably nourished the back limb and fore limb synclines. Later, sedimentation resumed, and the fold was draped by the Stephanian upper sub-sequence (Fig. 13c). The fan-shape geometry of these strata on SAR20 (Fig. 10b) suggest that sedimentation took place during the fold growth (Suppe and Medwedeff, 1990; Suppe et al., 1992; Hardy and Poblet, 1994; Ford et al., 1997; Butler et al., 2019).

Yet, this scenario must be investigated further since the fan-shape geometry is not observed on all the crosslines which rather suggest a post-compression deposition (drape strata). Nevertheless, our intra-Stephanian compression inferred fit with the proposal of Engel (1985) and Hertle and Littke (2000) which suggests that the Saarbrücken and the Simon thrust-fold formed during a Stephanian compression. This compression event corresponds to the Franconian compressional phase during the Stephanian or at the Stephanian-Autunian boundary (Stille, 1920; Pruvost, 1934; Kneuper, 1964; Gebhardt et al., 1991). Thus, the Stephanian period
511 was not governed by a global extension as proposed by many authors before. The formation of
512 the Stephanian half graben in the south-western part of the LCB (Hemelsdaël et al., 2023) might
513 have happened during the deposition of the drape strata overlying the ISU.

## 6. Conclusions

515 The study of gravity data has allowed to map the MHF and the top basement geometry while
516 the 2D seismic lines and wells has allowed to constrain the tectono-sedimentary evolution of
517 the Alsting thrust fold. These observations have led to the following conclusions:

518 • The MHFZ is a complex fault zone throughout the LCB and the SNCB with several
519 secondary branching faults which orientations varies laterally.

520 • The basement top map has shown the presence of basement highs (-1.5 km) and deeps
521 (-6.5 km) trending NE-SW, NNE-SSW to N-S and NW-SE. The NE-SW deeps align
522 with the piggyback and frontal synclines while the some of the NW-SE deeps align with
523 the known NW-SE Permian half-graben.

524 • The Alsting thrust-fold is a fault-propagation fold which formed during Stephanian.
525 Following its exhumation, the fold underwent an erosion leading to the development of
526 an intra-Stephanian unconformity (ISU) before the last phase of Stephanian subsidence.

527 • During this subsidence phase, the fold was sealed by drape strata (post-compressional)
528 overlaying the ISU. However, on SAR 20 seismic line striking parallel to the Alsting
529 thrust fold, the Stephanian growth strata overlaying the ISU may suggest that the Alsting
530 uplift was still active. This statement must be studied further.

531 • The combination of gravity, seismic and well data analysis has allowed to decipher a
532 different geological history of the LCB during Stephanian and have helped to constrain
533 the basement top structure which has received less attention until now.
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<figure><img src="image_2.png" /><figcaption>**Fig. 1.** The Lorraine Coal Basin (LCB) and the Saar Nahe Coal Basins (SNCB) within the Variscan orogeny units (modified from Franke, 2014).</figcaption></figure>

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<figure><img src="image_3.png" /><figcaption>**Fig. 2:** (a) Structural map of the LCB-SNCB (modified from Pruvost, 1934; Hannover, 1979; Donsimoni, 1981; Stollhofen, 1998; Hemelsdaël et al., 2023). The map is projected using the Lambert 93 system. (b) A Cross-section (grey line on (a)) at the France-Germany boundary showing the current geometry of the thrust-folds (modified from Juch et al., 1994).</figcaption></figure>

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<table><thead><tr><th colspan="2">TRIASSIC-MESOZOIC</th><th>Continental sub-stages</th><th>Thickness (m)</th><th>Lithology</th><th colspan="2">Depositional environments</th></tr><tr><th colspan="2">PERMIAN</th><th>Mid-Late</th><th></th><th>Non deposition/erosion</th><th colspan="2">Continental +Marine</th></tr><tr><th colspan="2">CARBONIFEROUS</th><th>Early</th><th>50-400</th><th></th><th>Reddish and greenish beds with less coal seams</th><th>Continental fluvio-lacustrine</th></tr></thead><tbody><tr><td rowspan="6">CARBONIFEROUS</td><td rowspan="6">Pennsylvanian</td><td>Early Stephanian</td><td>150-1600</td><td></td><td rowspan="6">Greyish beds rich in organic matter (coal seams)</td><td rowspan="6">Continental fluvio-lacustrine</td></tr><tr><td>Holz-conglomerate</td><td></td><td></td></tr><tr><td>Asturian (WD)</td><td>500-1100</td><td></td></tr><tr><td>Bolsovian (WC)</td><td>500-1400</td><td></td></tr><tr><td>Duckmantian (WB)</td><td>520</td><td></td></tr><tr><td>Langsettian (WA) Namurian</td><td>2000</td><td></td></tr><tr><td>Devonian-Visean</td><td>Emsian-Visean</td><td></td><td></td><td>Carbonates</td><td>Marine</td></tr><tr><td>Silurian-Devonian</td><td></td><td>Crystalline and metamorphic basement (Mid-German-Crystalline-High)</td><td></td><td></td><td></td><td></td></tr></tbody></table>

<figure><img src="image_4.png" /><figcaption>**Fig. 3.** Lithostratigraphy of the LCB with the different sub-stages defined in the Westphalian and Stephanian (modified from Donsimoni, 1981)</figcaption></figure>
<figure><img src="image_5.png" /></figure>

<table><thead><tr><th>Data</th><th>Facies % on each well</th><th>Base Depth (m)</th><th>Sonic velocities (m/s)</th><th>Time (s) after sonic</th><th>Time (s) on seismic lines</th></tr></thead><tbody><tr><td>Stages/ Borehole</td><td>Vaxy</td><td>Vaxy</td><td>Vaxy</td><td>Vaxy</td><td>Vaxy (LOR 09) (b)</td></tr><tr><td>Mesozoic</td><td>Cg(6)+Sa(43)+Cl(31)+Li(20)</td><td>800</td><td>2462</td><td>0.65</td><td>0.65</td></tr><tr><td>Permian</td><td>Sa(50)+Cl(50)</td><td>901</td><td>4040</td><td>0.7</td><td>0.7</td></tr><tr><td>Stephanian</td><td>Cg(5)+Sa(44)+Cl(43)+Co(8)</td><td>1001</td><td>4000</td><td>0.75</td><td>0.75</td></tr><tr><td>Westphalian D</td><td>Cg(1)+Sa(20)+Cl(73)+Co(6)</td><td>1652</td><td>3946</td><td>1.08</td><td>1.08</td></tr><tr><td>Stage / Borehole</td><td>Morhange</td><td>Morhange</td><td>Morhange</td><td>Morhange</td><td>Morhange (SAR20 and SAR1)</td></tr><tr><td>Mesozoic</td><td>Cg(7)+Sa(48)+Cl(26)+Li(19)</td><td>799</td><td>2663</td><td>0.6</td><td>0.6</td></tr><tr><td>Permian</td><td>Sa(75)+Cl(25)</td><td>1055</td><td>5120</td><td>0.7</td><td>0.7</td></tr><tr><td>Stephanian</td><td>Cg(2)+Sa(73)+Cl(25)</td><td>2268</td><td>4411</td><td>1.25</td><td>1.25</td></tr><tr><td>Westphalian D</td><td>Cg(6)+Sa(41)+Cl(48)+Co(5)</td><td>3000</td><td>4182</td><td>1.6</td><td>1.7</td></tr><tr><td>Stages/ Borehole</td><td>Germisay</td><td>Germisay</td><td>Germisay</td><td>Germisay</td><td>Intersection TOUL 12 /TOUL10</td></tr><tr><td>Mesozoic</td><td>Sa(20)+Cl(40)+Li(40)</td><td>1429</td><td>3572</td><td>0.8</td><td>0.8</td></tr><tr><td>Permian</td><td>Cg(30)+Sa(20)+Cl(50)</td><td>3429 (2757)</td><td>3400</td><td>2</td><td>2</td></tr><tr><td>Stephanian</td><td>Sa(60)+Cl(40)</td><td>6429</td><td>4000</td><td>3.5</td><td>3.5</td></tr></tbody></table>

Fig. 4. (a): Wells location on the structural map. Note also the location of the different NE-SW sub-stages thickness profiles from well data. These thickness profiles are presented on Figure.

The map is projected with Lambert 93 system explaining the gap of the X and Y coordinates locations. (b): Summary of the different parameters used in the seismic-to-well tie procedure.

Cg (conglomerate), Cl (claystone), Co (coal), Li (limestone) and Sa (sandstone).
<figure><img src="image_6.png" /><figcaption>**Fig. 5:** Map of the first vertical derivative highlighting the geometry of the MHFZ. Note the different abrupt changes of the MHFZ orientation from the SNCB to the LCB. The map is projected with the Lambert 93 system. The vertical and horizontal represent the grid used to compute the map and not the longitude and latitude lines. The later are represented by the cross visible on the map.</figcaption></figure>

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<figure><img src="image_7.png" /></figure>
**Fig. 6.** Map of the top of the basement under the LCB and the SNCB highlighting the presence of basement highs and throughs of different geometries, orientations and lengths. The map is projected with the Lambert 93 system. The vertical and horizontal represent the grid used to compute the map and not the longitude and latitude lines. The longitude and latitude lines are represented by the cross visible on the map. The Gironville (Gi) and the Saar-1 (Sa-1) wells that reach the basement are highlighted with bigger circles.
<figure><img src="image_8.png" /></figure>
**Fig. 7.** NE-SW well stratigraphy profiles in the LCB-SNCB highlighting the Mesozoic thickening toward the south-west, the Permian and the Stephanian thickening in syncline and their thinning or absence in the fold hinge areas.
<figure><img src="image_9.png" /><figcaption>(a) SAR 16</figcaption></figure>

<figure><img src="image_10.png" /><figcaption>(a) SAR 16</figcaption></figure>

<figure><img src="image_11.png" /><figcaption>(b) SAR 17</figcaption></figure>

<figure><img src="image_12.png" /><figcaption>(b) SAR 17</figcaption></figure>

<figure><img src="image_13.png" /></figure>

TMB : Triassic-Mesozoic Basis

PB : Permian Basis

ISU : Intra Stephanian Unconformity

CSB : Conformable Stephanian Basis

TWC : Top Westphalian C
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**Fig. 8:** (a) Uninterpreted and interpreted SAR16. (b) Uninterpreted and interpreted SAR17.

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These two lines highlight the structure of the Alsting anticline as a SE-vergent fault-propagation fold. Furthermore, note the presence of the ISU in the Stephanian sequence, separating a folded Early Stephanian sub-sequence with the non-folded sub-sequence. The ISU truncates the Westphalian D-Stephanian on the fold hinge.

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<figure><img src="image_14.png" /><figcaption>(a) SAR 18</figcaption></figure>

<figure><img src="image_15.png" /><figcaption>(b) SAR 5</figcaption></figure>

<figure><img src="image_16.png" /><figcaption>(a) SAR 18</figcaption></figure>

<figure><img src="image_17.png" /><figcaption>(b) SAR 5</figcaption></figure>

<figure><img src="image_18.png" /></figure>
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**Fig. 9.** (a) Uninterpreted and interpreted migrated SAR18. (b) Uninterpreted and interpreted migrated SAR5. The SAR18 highlights the same geometry observed on SAR16 and SAR17.

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The SAR5 line shows the ISU as a major intra-Stephanian post-folding erosion surface.

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<figure><img src="image_19.png" /><figcaption>(a) SAR 7</figcaption></figure>

<figure><img src="image_20.png" /><figcaption>(b) SAR20</figcaption></figure>

<figure><img src="image_21.png" /><figcaption>(a) SAR 7</figcaption></figure>

<figure><img src="image_22.png" /><figcaption>(b) SAR20</figcaption></figure>
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**Fig. 10.** (a) Uninterpreted and interpreted migrated SAR07. (b) Uninterpreted and interpreted migrated SAR20. The SAR7 highlights the Alsting fold as a pop-up anticline, probably a positive flower structure. The SAR20 shows that the Stephanian sub-sequence overlying the ISU is made up of typical growth strata.

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<figure><img src="image_23.png" /></figure>

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**Fig. 11.** (a) Uninterpreted and interpreted migrated RE01. (b) Uninterpreted and interpreted migrated RE04. The RE01 highlights the Merlebach anticline as a SE-vergent thrust fold with

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884 Stephanian sequence in the Landroff syncline. The RE04 highlights NW-SE syn- Stephanian
885 sedimentary faults.

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<figure><img src="image_24.png" /></figure>

<figure><img src="image_25.png" /><figcaption>**Fig.12.** (a). Location of the different seismic lines and wells highlighted in b. (b). Two-Way-Time (from seismic) and depth profile of the Top Westphalian D from the Alsting to the Morhange thrust-folds highlighting the Morhange growth syncline between the two thrust-folds and the same growth strata on the LOR9 seismic line from Hemelsdaël et al. (2023).</figcaption></figure>

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<figure><img src="image_26.png" /></figure>

**Fig. 13.** Proposal of a tectono-sedimentary evolution of the Alsting anticline. The cross-sections are not in scale. (a) Continuous deposition from the Westphalian until the Early Stephanian lower sub-sequence. (b) Thrusting and folding of the Westphalian-Stephanian sub-sequence leading to the formation of the Alsting thrust fold and its subsequent uplift and erosion. (c) Renew of subsidence and deposition of the Upper Stephanian sub-sequence as drape strata.