Sedimentary Stylolites Roughness Inversion Enables the Quantification of the Eroded Thickness of Deccan Trap Above the Bagh Group, Narmada Basin, India

Abstract

Stylolites, common dissolution surfaces in carbonate rocks, form due to localized stress-induced pressure-solution during burial compaction or tectonic contraction. Their morphology and growth are influenced by dissolution kinetics, rock heterogeneity, clay content, burial depth, stress evolution, diagenesis, and pore fluid availability. This study applies the stylolite roughness inversion technique (SRIT), a proven paleopizometer that quantifies the principal vertical stress (σ_v = σ₁) prevailing in strata in the last moments of bedding-parallel stylolites (BPS) formation, to the Late Cretaceous Bagh Group carbonates in the Narmada Basin, India, to estimate their burial paleo-depth. Using the Fourier Power Spectrum (FPS), we obtained 18 σ₁ values from a collection of 30 samples, enabling us to estimate paleo-burial depths for the Bagh Group ranging from 660 to 1320 m. As the Bagh Group burial history is unknown, but as there is no subsequent sedimentary deposition above it, we relate this ca. 1.3 km burial depth to the now eroded thickness of the deposits related to Deccan volcanism at the end of the Cretaceous time, implying a quasi-instantaneous development of the BPS population in the strata. This research highlights the robustness of SRIT for reconstructing burial histories in carbonate sequences and that it can be a reliable way to reconstruct the thickness of eroded deposits in well-constrained geological history.

1. Introduction

Stylolites are rough dissolution surfaces commonly found in carbonate rocks within sedimentary basins formed by localized stress-induced pressure-solution during burial-related compaction or tectonic contraction [1,2,3,4]. They are visible in cross-section as serrated lines or ridges due to the accumulation of less soluble materials (clay, mica, and oxides) with asperities ranging from micrometers to centimeters [5]. Stylolite growth and morphology are rate-dependent, governed by dissolution kinetics [6], heterogeneity distribution, and clay content [7]. Furthermore, burial depth, basin stress evolution, diagenetic overprinting, and the availability of pore fluids also influence stylolite formation [8,9]. Depending on their permeability and sealing properties, stylolites can either accelerate diagenetic reactions by acting as fluid conduits, have no impact, or inhibit reactions by functioning as barriers, thereby influencing the spatial distribution of diagenetic products [10,11,12].

The roughness is defined as the difference in height (dh) between two points, separated by a defined horizontal distance (dx) along the stylolite track. Stylolite track roughness, characterized by its scale-invariant (self-affine) geometry in 1D, serves as a valuable paleostress indicator because its final form reflects the ambient stress magnitude at fossilization, i.e., the time pressure-dissolution stopped, independent of strain rate or lithology, effectively capturing a snapshot of those past conditions [7,13]. The Stylolite Roughness Inversion Technique (SRIT), a method leveraging stylolite roughness as a paleopiezometer, quantifies principal vertical stress (σ1) when applied to bedding-parallel stylolites (BPS) to estimate the maximum burial depth. Numerous recent works have successfully applied it to various basins around the world and in various settings. In cases where there are no (or not much) tectonics, SRIT applied to BPS returns a depth equivalent to the maximum depth of burial experienced by the host strata [8,14,15,16]. In cases where the basin underwent deformation (e.g., in foreland basins, stressed passive margins, Fold-and-Thrust Belts), SRIT returns a depth that can be interpreted as an access to the maximum pre-contraction depth [17,18,19,20,21,22,23]. Such regional results were always cross-validated by comparison to local estimates of paleo-depth. Yet, over the past decade, methodological efforts were dedicated to validate the applicability of SRIT in various environments against (1) comparison with indirect measurements of the maximum burial depth using organic or inorganic thermal indicator [8,19], (2) comparison to direct age measurements in structures developed after σ1 was no longer vertical [17,21] and (3) by direct measurement of the temperature at which BPS developed [18]. Considering the success of these previously published validations, SRIT should be used as a standalone methodology to reliably assess the first-order depth of burial of the strata, of which the interpretation (maximum versus intermediate depth) is dependent on the regional geological history.

This research aims to estimate burial depth in carbonate rocks using the Stylolite Roughness Inversion Technique (SRIT) on bedding parallel stylolites (BPS) from the Bagh Group of the Narmada Basin, India [24]. In such a basin, when no study on organic matter maturity is available, we test SRIT for a blind determination of burial paleo-depth in rocks that were affected by stylolitization when subjected to vertical stress. The burial depth of the host carbonates is calculated by reconstructing vertical stress from BPS data using the Fourier power spectrum (FPS) analysis [7,13,14,16,17,22,25,26,27], and the implication of these depths is further discussed with respect to the diagenetic and geological history of the area.

2. Geological Context

The Narmada Graben, situated along the northern flank of the Satpura horst, stands out for its elevated heat flow [28]. This tectonic configuration, with Satpura forming a horst and the adjacent Narmada and Tapi valleys manifesting as grabens (Figure 1B,C), has been substantiated by seismic refraction and wide-angle reflection studies [29]. The bounding faults of the Narmada Graben are steep, dipping at 70–80° (Figure 1D) [30], and show a cumulative displacement of around 1500–1800 m [31].

The carbonate sequence of the Bagh Group of the Narmada Basin in central India represents the epicontinental basin deposits of the Late Cretaceous marine inundation of the Indian subcontinent.

2.1. Lithostratigraphy of the Bagh Group

The Cenomanian fluvio-marine siliciclastic Nimar Formation is overlain by marine carbonates of the Turonian Nodular Limestone Formation and the Coniacian Bryozoan Limestone Formation. At the regional scale, the carbonate deposits are overlain by the Maastrichtian fluvio-marine, siliciclastic Lameta Formation or by flood basalts of the Deccan Traps (Figure 1A), which are absent in the basin but have an estimated thickness of about 1.8 km in the surrounding area [36].

2.2. Facies Constituting the Carbonate of Bagh Group

The Bagh Group comprises several facies described [24] and summarized hereinafter. Nodular Limestone Formation is represented by three non-repetitive facies: (i) Facies A—Wackestone–mudstone alternations, (ii) Facies B—Nodular wackestone, and (iii) Facies C—Poorly bedded wackestone. The overlying Bryozoan Limestone Formation (also known as Coralline Limestone, Barwah Bryozoan Limestone, and Chirakhan Limestone) consists of three facies: (i) Facies D—Cross-stratified rudstone, (ii) Facies E—Planar laminated rudstone, and (iii) Facies F—Faintly laminated packstone in ascending order.

Three distinct hardgrounds are present in ascending stratigraphic order: the first (Hardground 1), a 20 cm thick, brownish to pinkish yellow, extensively burrowed, bored (by Gastrochaenolites and Trypanites), and encrusted surface atop the nodular wackestone of the Nodular Limestone Formation; the second (Hardground 2), a 20 cm thick, rust brown, Fe-oxide impregnated layer at the top of this formation, separating it from the overlying Bryozoan Limestone and exhibiting bored bioclasts (echinoderm and bryozoan remains), Gastrochaenolites burrow erosion, truncation, and encrustation by Chiplonkarina and oysters; and the third (Hardground 3), within the Bryozoan Limestone, atop a cross-stratified Bryozoan Limestone unit, marked by Fe-oxide impregnated Thalassinoides burrows and transitioning upward into firmgrounds. Brief description and process interpretation of these facies are given below.

Wackestone–mudstone alternations: This facies consists of dark gray to pinkish gray colored wackestone–mudstone alternations about 1.7 to 3.1 m thick with parallel to wavy bed geometry, characterized by a lack of primary depositional sedimentary structures and a paucity of fossils with low degree of bioturbation and desiccation cracks. The wackestone beds often contain pisoids, intraclasts, and relics of bioclasts such as gastropods, echinoderms, molluscs, and forams with abundant calcispheres. A low-energy, upper intertidal to supratidal depositional environment that undergoes frequent subaerial exposures.

Nodular wackestone: Varying in thickness from 1.6 m to 2.9 m, this facies consists of nodular wackestone, locally grading to packstone, and is distinguished by desiccation cracks, root structures, a rich assemblage of invertebrate fossils (including bored and fragmented shells), in situ brecciated rootlets, rhizoconcretions with alveolar–septal texture, invertebrate borings, and Thalassinoides burrows. The nodules, primarily composed of lime mudstone and ranging in shape from broadly spherical (3–7 cm diameter) to ellipsoidal, are embedded within a matrix predominantly consisting of micrite rich in well-preserved bioclasts such as gastropods, echinoderms/echinoid spines, and molluscs, reflecting the abundance of micrite and poor sorting of the bioclasts. The low-energy shallow marine platform—tidal flat depositional condition with long periods of subaerial exposure and pedogenesis.

Poorly bedded wackestone: This facies consists of crudely laminated or massive wackestone characterized by distinct flattened nodularity in which nodules are isolated to be jointed and wrapped by thick seams of high proportion of argillaceous material. The thickness of the facies varies from 1.3 m to 2.4 m and exhibits alveolar texture and intensive calcification. Bioclasts, mainly gastropod, bivalve, and rare foraminifera, occur in patches and are frequently impregnated by Fe-oxides. A low-energy environment of deposition, along with pedogenesis during long periods of subaerial exposure.

Cross-stratified rudstone: Reddish brown to whitish-brown, thick- to thin-bedded rudstones, characterized by trough and planar cross-stratification with a weakly bipolar, flood-tide dominated paleocurrent pattern, comprise these facies, which contain fragmented bryozoans, echinoids, brachiopods, bivalves, and gastropods, are well-sorted with no micrite, and are occasionally bioturbated by Thalassinoides. High-energy depositional environment characteristic of the lower intertidal environment.

Planar laminated rudstone: The facies consists of greenish gray, planar laminated rudstone, ranging from 20 cm to 1.3 m thick, characterized by dissolved and strongly bored bioclasts with Fe-oxide coatings and intense micritization; microscopic analysis revealed abundant skeletal grains, including fragments of echinoderms (e.g., echinoid spines), bryozoans, gastropods, ostracods, brachiopods, mollusks, and foraminifera, within a matrix containing moderate amounts of feldspar and quartz, along with 10%–25% glauconite. A high-energy depositional condition of a lower intertidal depositional setting.

Faintly laminated packstone: The facies, ranging from 1 to 1.5 m in thickness, are dominantly composed of poorly bioturbated, fossiliferous packstone with a grain-supported fabric. Well-sorted allochems are a key feature, along with Thalassinoides burrows, abundant meniscus cement, and biomolds. Bioclasts, including bryozoans, echinoderms, and bivalves, make up a significant portion of the rock (up to 80%). Moderate energy depositional conditions in near-shore environments are related to lower intertidal deposits.

A low-energy, restricted, shallow, marine-platform, tidal flat system (ranging from supratidal to upper intertidal), subject to periodic subaerial exposures, is inferred for the deposition of the Nodular Limestone. This environment is suggested by the dominance of fine-grained carbonates and mud, the presence of well-preserved small body fossils, and the overlying carbonate units, which signify a reduction or cessation of clastic input in the post-Nimar transgressive depositional system. On the other hand, the presence of abundant cross-stratified/plane-laminated rudstone with siliciclastics, rare mud content, and well-sorted bioclasts in the Bryozoan Limestone provides strong evidence for a high-energy, shallow marine (lower intertidal channels) depositional environment [24,37,38,39,40]. The presence of three hardgrounds within the carbonate sequence—primarily marking surfaces of non-deposition—and the associated pattern of slow water-level rise (transgressive trend) followed by a sharp drop suggest an asymmetric depositional cycle.

3. Materials and Methods

3.1. Stylolites in the Carbonate of Bagh Group

A series of 30 bedding-parallel stylolites were sampled throughout the rock units in several points of the basin (Figure 1B) for subsequent petrographic investigation, morphology, and roughness characterization.

The carbonate rock of the Bagh Group exhibits a dispersed distribution of stylolites, ranging from microscopic to macroscopic. Three distinct stylolite connectivity types—isolated, long-parallel, and anastomosing networks (Figure 2, Figure 3 and Figure 4) determine the potential for fluid flow in rocks, a parameter influenced by not only stylolite morphology but also wavelength, amplitude, and orientation [9].

Following the classification of [4], we recognized stylolites with diverse morphologies, including seismogram pinning (Class 2) type (Figure 5B), suture and sharp peak (Class 3) type (Figure 5A and Figure 6A,C), and simple wave (Class 4) type (Figure 2C and Figure 6D).

3.2. Methodology for Stress Inversion

Stylolite roughness can be studied as a 2D track on a polished cross-section cut perpendicular to the stylolite’s plane [7] to assess the magnitude of the principal stress striking parallel to the stylolite’s teeth [13]. To achieve this, SRIT [41] consists of performing signal analysis on the roughness, i.e., the difference in height between two consecutive points constitutive of the track can be studied as a signal, with various spatial frequencies corresponding to the horizontal distance between the consecutive points [13].

The method is based on a model where stylolite’s growth is balanced between the two stabilizing forces—one is long-range elastic fluctuation, and the other is local surface tension—and a destabilizing force related to pinning particles [13]. As the main destabilizing force depends on the scale of observation, there is, in the spectral domain, a characteristic length at which the regime developing roughness switches from being controlled by the elastic forces to being controlled by the local surface tension. This length is a key factor named the Crossover Length (L_c), which depends on both mean and differential stress under which the roughness is developed as follows:

$${\mathrm{L}}_{\mathrm{c}}={\displaystyle \frac{\mathsf{\gamma }\mathrm{E}}{\mathsf{\beta }{\mathsf{\sigma }}_{\mathrm{m}}{\mathsf{\sigma }}_{\mathrm{d}}}}$$

(1)

where L_c is crossover length, E is Young’s Modulus, $\mathsf{\gamma }$ is solid–fluid interfacial energy, and $\mathsf{\beta }={\displaystyle \frac{\mathsf{\upsilon }(1-2\mathsf{\upsilon })}{\mathsf{\pi }}}$ is a dimensionless constant. $\mathsf{\upsilon }$ is Poisson’s ratio and ${\mathsf{\sigma }}_{\mathrm{d}}$ and ${\mathsf{\sigma }}_{\mathrm{m}}$ are differential stress and mean stress, respectively.

In other words, SRIT can return stress magnitude at the time a stylolite stopped developing. In a Fourier domain on a log–log plot (using FPS—Fourier Power Spectrum), both the roughness controlled by elastic and surface energy are defined by a straight line with a different slope [7,13]. This slope is defined by the Hurst Coefficient (H), a transferable coefficient determined for the FPS as a power law exponent of P(k) = k^−(1+2H), depending on the origin of the phenomenon it describes, with capillary effects mainly dominant when H > 1(here mainly 1.1) at short length scale whereas H < 1 (Here mainly 0.5) the stress distribution may control the geomorphometry of stylolites during formation at large scale length [7].

When applied to bedding parallel stylolites (BPS), that developed under a maximum principal stress being vertical, it is possible to assume that both horizontal stresses are of the same value (uniaxial strain hypothesis), leading to a simplification of Equation (1) as follows [14]:

$${\mathrm{L}}_{\mathrm{c}}={\displaystyle \frac{\mathsf{\gamma }\mathrm{E}}{\mathsf{\beta }\mathsf{\alpha }{\mathsf{\sigma }}_{\mathrm{z}\mathrm{z}}^2}}$$

(2)

where $\mathsf{\alpha }={\displaystyle \frac{1\left(1+\mathsf{\upsilon }\right)(1-2\mathsf{\upsilon })}{3(1-\mathsf{\upsilon })(1-\mathsf{\upsilon })}}$ and $\mathsf{\beta }={\displaystyle \frac{\mathsf{\upsilon }(1-2\mathsf{\upsilon })}{\mathsf{\pi }}}$.

Then, one can derive the depth z at which the stylolite’s growth stopped by using $\mathsf{\rho },$ the average density of the rock column above the studied strata, and g, the acceleration of gravitational forces, as follows:

$${\mathsf{\sigma }}_{\mathrm{v}}=\mathsf{\rho }\mathrm{g}\mathrm{z}$$

(3)

Previous parametric studies suggested that the selection of suture and sharp peak-type stylolites for maximum paleo-depth determination, suture and sharp peak stylolite types (class 3) are optimal, whereas seismogram pinning stylolites (class 2) yield intermediate depth estimations [8,19].

3.3. Applicability to the Bagh Group Formations

Here, we studied nearly 30 BPS (Bedding Parallel Stylolites) collected from hand samples of Bryozoan Limestone from the Bagh Group (Figure 1). Following what was recalled previously, the sampling focused on class 2 (seismogram pinning) and class 3 (suture and sharp peak) stylolites. Selected hand samples were cut perpendicular to the stylolite track, ensuring the peak of the stylolite was locally perpendicular to the dissolution plane in 2D. Cuts were polished to remove the clay from the samples and then scanned using a high-resolution 2D scanner (3200 dpi), corresponding to a pixel size of 8 µm. The track of each stylolite was then digitized by hand using the pencil tool (thickness 5.00) with a 400% magnification in GIMP 2.10.38. We used the Matlab script developed by [14,26], updated by [21,22]. It involves a non-linear regression of fixed slopes (1.1 and 0.5) that enables them to find the slope break (Lc) within 23% uncertainties. According to [20], the propagation of this uncertainty into Equation (2) leads to estimates of σ_v within 12% uncertainty, providing no major error is made on the other parameters.

Consequently, in order to perform the inversion to stress, we estimated the Young’s modulus (E), which is considered the most uncertain elastic parameter for carbonate rocks [42], using the Schmidt hammer. It is a measure of the rebound value (R) of a spring-loaded piston when applied orthogonally to the rock surface. This R value scales with the Young modulus of the rock, following E = 0.00013 × R^3.090704 [43]. Other parameters involved in Equations (2) and (3) are well-constrained in carbonate rocks. Thus, we consider $\mathsf{\gamma }$ = 0.23 J/m² [44] and Poisson’s ratio $\mathsf{\upsilon }$ = 0.25 $\pm$ 0.05 [45]. Lastly, we calculate the paleostress burial depth (z) considering the density of potentially overlying rocks ($\mathsf{\rho }=$ 2700 Kg/m³) and g = 9.81 m/s².

4. Results

Out of the 30 collected samples, 18 BPS returned a valid inversion (Figure 1C), i.e., two slopes well defined by the two Hurst exponents of 1.1 and 0.5 (Figure 7,

Table 1. Results from the application of the stylolite roughness inversion technique (SRIT) on samples of the Bagh Group, Narmada Basin, India. * FPS (Fourier Power Spectrum) inversion results using γ = 0.23 J/m² [44], Poisson’s ratio υ = 0.25 ± 0.05 [45], E (Young’s Modulus) = 25 GPa, (density) of rock $\rho$ = 2700 Kg/m³, g = 9.81 m/s². All stress and depth values are given without the 12% uncertainty, while Lc values are reported without the 23% uncertainty.

Sample No.	Location	Lat (°N) and Long (°E)	Morphology Class	Stylolite Length (mm)	Crossover Length Lc (mm)	Paleostress * (MPa)	Depth * (m)
BG001	Kasdana	22.24 and 74.93	3	20	0.572	26	910
BG002	Kasdana	22.24 and 74.93	3	18	0.41	31	1090
BG003	Kasdana	22.24 and 74.93	3	18	0.32	35	1230
BG004	Kasdana	22.24 and 74.93	3	15	0.34	34	1200
BG005	Kasdana	22.24 and 74.93	3	25	0.748	23	810
BG006	Kasdana	22.24 and 74.93	3	16	0.596	26	910
BG007	Kasdana	22.24 and 74.93	3	20	1.225	18	630
BG008	Kasdana	22.24 and 74.93	3	20	0.864	21	740
BG009	Kasdana	22.24 and 74.93	2	25	0.609	25	880
BG010	Kasdana	22.24 and 74.93	3	25	0.89	21	740
BG011	Kasdana	22.24 and 74.93	3	14	0.572	26	910
BG012	Karondia	22.38 and 74.07	3	14	0.34	34	1200
BG013	Karondia	22.38 and 74.07	3	16	0.39	32	1120
BG014	Karondia	22.38 and 74.07	3	18	0.472	29	1020
BG015	Zirabad	22.41 and 75.07	2	18	1.27	18	630
BG016	Zirabad	22.41 and 75.07	3	20	0.47	29	1020
BG017	Zirabad	22.41 and 75.07	3	18	0.69	24	840
BG018	Ratitalai	22.40 and 75.05	3	30	0.830	22	770

). L_c values vary from 0.31–1.26 (Figure 7), with no clear relationship to the relative depth of sampling if considering the Bagh Group. For conducting the inversion from L_c to stress, we assumed the horizontal in-plane stress was negligible. The values for Young’s Modulus, by far the biggest source of uncertainty in SRIT [22,27], were estimated through the rebound value obtained with the Schmidt Hammer. A total of 45 R values were obtained from flat, homogeneous surfaces across 31 samples of Bagh Carbonate rock. These R values are strikingly consistent and range from 21 to 22, resulting in calculated Young’s moduli between 22 and 25 GPa [43].

Solving Equation (3) for each Lc value, we obtain a paleo burial depth varying between 670 and 1320 m with a median value of 970 m, and first and last quartiles of 810 and 1180 m, respectively (rounded to the closest 10 m, excluding the 12% uncertainty, Table 1).

5. Interpretation

The morphological variability of stylolites within sedimentary rocks, characterized by wavelength, frequency, and amplitude across multiple scales, exerts a significant influence on both the efficiency of fluid flow along dissolution planes and the accurate estimation of chemical compaction [4,6]. The morphology of stylolites is controlled by both growth regimes [4] and the distribution of heterogeneity within the host rock [46]. To ensure that the recorded depth through SRIT is consistent, we analysed suture and sharp peak (Class 3) stylolites [4]. In the Late Cretaceous, carbonates of the Bagh Group were initially deposited in the basin due to marine transgression. Subsequently, its properties were altered by bioturbation. As burial progressed (a few hundred meters), overburden pressure increased (σ₁ = σ_v), and pressure solution was initiated, leading to the formation of stylolites. As our dataset suggests, stylolitization was intense up to 1000 m depth, resulting in extensive stylolitization in the lower layers, marked by closely spaced, well-developed stylolites, reflecting significant volume reduction (Figure 8).

6. Discussion

6.1. Burial Depth

Bedding parallel stylolites develop under a vertical principal stress, and stop developing for various reason, including a rise in local fluid pressure [19], decrease in the solubility gradient by clay accumulation [3], deepening of the strata and accommodation of shortening by more efficient dislocation/recrystallisation mechanisms [10], or change in the tectonic stress regime [47]. This case study reconstructed depth ranging from 600 to 1500 m within the 12% uncertainty for the stress calculations [27], and because we do not have an independent estimate of the expected maximum burial depth, it is hard to explain why BPS halted their development. Indeed, the Bagh Group is the last formation before the Deccan Traps were deposited [48]. As a large portion of the related lava was eroded since deposition, we know that the studied area was covered [49], but we do not know what the thickness of this magmatic cover was. Yet, the Bagh Group carbonates’ own thickness does not allow the explanation of the minimal burial depth of 1500 m when BPS stopped developing. On top of it, one can note that the maximum reconstructed depth is not found only at the bottom of the Bagh Group (BG2–4; BG 12–13, Table 1, Figure 1). So, this range of values probably reflects a sequential stop of BPS activity [18] rather than a synchronous stop at the scale of the whole formation [14]. However, the range of depth reconstructed from SRIT is in agreement with the thickness of the Deccan Traps deposited around the basin but likely eroded in the basin, with a present-day thickness of 700 m to 2 km (average 1.8 km, [36]). We then propose that a minimum of 1.3 km of volcanic material was deposited at the scale of the Narmada Basin, on top of the Bagh Group, and developed a dense stylolite network during the catastrophic accumulation of the traps, i.e., likely under 600 Kyr [50]. This is a minimum thickness because BPS could have stopped developing before strata reached the maximum burial depth.

6.2. About the Duration of Stylolite Development

Stylolites are important microstructures that can significantly alter the fluid flow in carbonate reservoirs [12,51]. Hence, understanding the duration of their development is an important yet elusive and challenging problem. In the literature, comparing the result of SRIT to a burial model enable to estimate the time span during which BPS developed, continuously or not: it is about 50 Myr in the Paris Basin [8], about 150 Myr in the Bighorn Basin (USA, [17]), between 10 and 6 Myr in the Umbria Marches [21], and about 20 Myr in the Lower Congo Basin [19,20]. In the Mirabeau Anticline [52], U-Pb radiochronology was used on syn-solution cements located at the tips of different BPS in the same hand sample and results show that these BPS developed at least 20 Myr apart from each other. These durations contrast with the present case study: one can consider the 1.3 km burial depth as a minimum burial depth, because up to 2 km of volcanic material could have been deposited in the area [36]. If meaningful, this difference implies that all the studied stylolites developed before the complete thickness of the traps was deposited. That brings new constraints to the timescale of stylolite development in nature, suggesting that a complete population of stylolites can develop in less than 1 Myr. In other words, in this case, BPS developed at a quasi-instantaneous rate considering the geological timescale. When studying the BPS depth of development in the Western African Margin, the population of BPS studied by [52] with SRIT highlighted a bimodal distribution of the Lc, leading to the observation of a maximum of stylolite developed during a fast burial phase before 95 Ma while the rest of the population developed after 35 Ma, under a gentler burial rate. The authors suggested that a correlation between burial rate and stylolite development could exist. In literature, no data can allow to independently estimate the timespan of BPS development from the burial rate but the present study, then, it is limiting our capacity to validate if there is a positive correlation between the burial rate and the development of a BPS population (i.e., in other studies, the timespan is estimated from the burial curves). The present case study highlights that it might be possible to develop a big network of BPS in a very short timespan and with a very high burial rate (ca. 2.5 km/Myr). This, in our opinion, raises a challenging question to investigate further.

7. Conclusions

The Late Cretaceous carbonate lithologies of the Bagh Group, situated within the Narmada Basin, exhibit a prevalence of bedding-parallel stylolites of variable dimensions. Morphological analysis of the stylolites present in the Bagh Group’s carbonate rocks reveals two most distinct categories: (a) suture and sharp peak type stylolites, and (b) simple wave type stylolites.

The application of roughness inversion methodology to these stylolites enables the estimation of sedimentary stylolite formation depth, thereby facilitating the reconstruction of stratigraphic burial history. The principal vertical stress and corresponding burial depth are determined by utilizing the suture and sharp peak-type stylolites, which are dominant in the carbonate rocks in the Bagh Group.

The application of the FPS methodology to 18 bedding-parallel stylolite datasets derived from the carbonate lithologies resulted in a heterogeneous distribution of inferred burial depths ranging from 670−1320 m, with a median value of 970 m, independently of the stratigraphic position of samples in the Bagh Group. The calculated depths imply reevaluating the burial history of the Narmada Basin, considering the important role of the now eroded Deccan Traps in the area.

Beyond regional implication, this study is the first to rely on BPS SRIT only to reconstruct burial in a basin, and it clearly illustrates that BPS inversion for vertical stress can be used to serve as a gauge for the minimal thickness of eroded formation and can even guide reconstruction of past eruptive events in both intensity and geographical extent.