Vincenzo La Bruna

Juliette Lamarche

Fabrizio Agosta

Andrea Rustichelli

Alessandro Giuffrida

Roland Salardon

Lionel Marié

Structural diagenesis of shallow platform carbonates: Role of early embrittlement on fracture setting and distribution, case study of Monte Alpi (Southern Apennines, Italy)

Keywords: Fractures, Carbonates, Early cementation, Diagenesis, Reservoirs, Southern Apennines, µ

ou non, émanant des établissements d'enseignement et de recherche français ou étrangers, des laboratoires publics ou privés.

Introduction

Carbonate reservoirs are of a great importance for hydrocarbon exploitation, water resource, and gas sequestration (Barlét-Gouédard et al., 2006;[START_REF] Ford | Karst hydrogeology and geomorphology[END_REF][START_REF] Ahr | Geology of carbonate reservoirs: the identification, description and characterization of hydrocarbon reservoirs in carbonate rocks[END_REF]. These reservoirs are very often characterized by both primary and secondary heterogeneities [START_REF] Nelson | Geologic analysis of naturally fractured reservoirs[END_REF][START_REF] Lucia | Carbonate reservoir characterization: An integrated approach[END_REF], which occur from regional (100's of m to km), to outcrop (cm to 100 m) and micro-scale (mm to cm).

In reservoir modelling, heterogeneities with dimensional properties smaller than 10m are included into the matrix properties, leading to quite unrealistic scenarios in the case of fractured carbonates, which have been subjected to complex diagenetic and tectonic histories [START_REF] Warren | The behavior of Naturally Fractured Reservoirs[END_REF][START_REF] Barbier | Sedimentary and diagenetic controls on the multiscale fracturing pattern of a carbonate reservoir[END_REF][START_REF] Matonti | Heterogeneities and diagenetic control on the spatial distribution of carbonate rocks acoustic properties at the outcrop scale[END_REF][START_REF] Giorgioni | Impact of early dolomitization on multi-scale petrophysical heterogeneities and fracture intensity of low-porosity platform carbonates (Albian-Cenomanian, southern Apennines, Italy)[END_REF][START_REF] Panza | Fracture stratigraphy and fluid flow properties of shallow-water, tight carbonates: the case study of the Murge Plateau (southern Italy)[END_REF]Giuffrida et al., 2019a). Particularly in tight carbonates, both outcrop-scale and micro-scale fractures may drive a large amount of geofluids [START_REF] Guerriero | A permeability model for naturally fractured carbonate reservoirs[END_REF][START_REF] Anders | Microfractures: A review[END_REF][START_REF] Panza | Meso-to-microscale fracture porosity in tight limestones, results of an integrated field and laboratory study[END_REF]. Since cementbearing fractures are widespread in the subsurface, fluid can only flow where fractures are now days barren or partly cemented [START_REF] Aguilera | Geologic aspects of naturally fractured reservoirs[END_REF][START_REF] Nelson | Geologic analysis of naturally fractured reservoirs[END_REF][START_REF] Laubach | Practical approaches to identifying sealed and open fractures[END_REF][START_REF] Matonti | P-wave velocity anisotropy related to sealed fractures reactivation tracing the structural diagenesis in carbonates[END_REF]. Hence, deciphering the interaction between fractures and diagenesis is a key point for a good understanding of the reservoir properties. Accordingly, the assessment of fracture timing and sealing due to cementation is of a prime importance for fractured carbonate reservoir analysis [START_REF] Laubach | Structural diagenesis[END_REF]Vitale et al., 2012). In the last decade, the few studies that focused on the relationships between structural and diagenetic processes in carbonates pointed out the possible occurrence of a early embrittlement [START_REF] Frost | Controls on syndepositional fracture patterns, Devonian reef complexes, Canning Basin, Western Australia[END_REF][START_REF] Lavenu | Tectonic versus diagenetic origin of fractures in a naturally fractured carbonate reservoir analog (Nerthe anticline, southeastern France) Tectonic Vs. Diagenetic Fractures in a Naturally Fractured Reservoir[END_REF][START_REF] Lavenu | Relating background fractures to diagenesis and rock physical properties in a platform-slope transect. Example of the Maiella Mountain (central Italy)[END_REF]Lamarche 2015a;Lamarche et al., 2015b;[START_REF] Tavani | Introducing dolomite seams: hybrid compaction-solution bands in dolomitic limestones[END_REF][START_REF] Vinci | Early dolomitization in the Lower Cretaceous shallow-water carbonates of Southern Apennines (Italy): Clues about palaeoclimatic fluctuations in western Tethys[END_REF][START_REF] Lavenu | What controls diffuse fractures in platform carbonates? Insights from Provence (France) and Apulia (Italy)[END_REF]. Along this line, the analysis of outcrop analogues of subsurface fractured carbonates is often employed to lower the uncertainties and bias associated to reservoir characterization and modelling [START_REF] Lamarche | Relationships between fracture patterns, geodynamics and mechanical stratigraphy in Carbonates (South-East Basin, France)[END_REF][START_REF] Rustichelli | Spacing and distribution of bed perpendicular joints throughout layered, shallow-marine carbonates (Granada Basin, southern Spain)[END_REF][START_REF] Agosta | The role of mechanical stratigraphy on normal fault growth across a Cretaceous carbonate multi-layer, central Texas (USA)[END_REF][START_REF] Lavenu | Background fractures in carbonates: inference on control of sedimentary facies, diagenesis and petrophysics on rock mechanical behavior. Example of the Murge Plateau (southern Italy)[END_REF][START_REF] Corradetti | Distribution and arrest of vertical through-going joints in a seismicscale carbonate platform exposure (Sorrento peninsula, Italy): insights from integrating field survey and digital outcrop model[END_REF][START_REF] Guerriero | The role of stratabound fractures for fluid migration pathways and storage in well-bedded carbonates[END_REF][START_REF] Panza | Fracture stratigraphy and fluid flow properties of shallow-water, tight carbonates: the case study of the Murge Plateau (southern Italy)[END_REF][START_REF] Panza | Discrete Fracture Network modelling of a hydrocarbon-bearing, oblique-slip fault zone: Inferences on fault-controlled fluid storage and migration properties of carbonate fault damage zones[END_REF]Panza et al., , 2019;;[START_REF] Massaro | Multiscale Fracture Analysis in a Reservoir-Scale Carbonate Platform Exposure (Sorrento Peninsula, Italy): Implications for Fluid Flow[END_REF]Giuffrida et al., 2019a). In this paper, we investigate the polyphase diagenetic history of fractures crosscutting shallow-water platform carbonates of Monte

Accepted Manuscript

Alpi, southern Italy [START_REF] Sartoni | Ricerche biostratigrafiche nel Mesozoico dell'Appennino Meridionale[END_REF][START_REF] Corrado | Tectonic burial and exhumation in a foreland fold and thrust belt: The Alpi Mt. case history (Southern Apennines, Italy)[END_REF][START_REF] Shiner | Thin-skinned versus thick-skinned structural models for Apulian Carbonate Reservoirs: constraints from the Val D'Agri Field[END_REF][START_REF] Mazzoli | Pliocene-Quaternary thrusting, synorogenic extension and tectonic exhumation in the southern Apennines (Italy): Insights from the Alpi Mt. area. In Styles of Continental Contraction[END_REF][START_REF] Mazzoli | Tectonic burial and "young" (< 10 Ma) exhumation in the southern Apennines fold-and-thrust belt (Italy)[END_REF][START_REF] Bruna | New insights on the structural setting of the Monte Alpi area, Basilicata, Italy[END_REF], 2018). This massif can be considered as a good structural analogue for nearby oil fields of the Basilicata Region, as well as a case study for a multi-scale analysis of carbonate reservoirs involved in a complex tectonic history. In light of their time-dependant tectonic evolution, the goal of the present work is to assess the control exerted by carbonate facies on the structural diagenesis of the Lower Cretaceous limestones.

Geological setting

The Apennines are an arc-shaped fold-and-thrust belt (FTB) due to the Oligocene-to-Pleistocene continental collision between Eurasian and African plates (Patacca and Scandone, 2007, and references therein). Contractional deformation was characterized by the eastward propagation of thrust sheets, which involved Meso-Cenozoic sedimentary successions originally pertaining to the Neo-Tethys Ocean due to the rollback of the Adriatic slab [START_REF] Royden | Segmentation and configuration of subducted lithosphere in Italy: An important control on thrust-belt and foredeep-basin evolution[END_REF][START_REF] Patacca | Tyrrhenian basin and Apenninic arcs: kinematic relations since late Tortonian times[END_REF][START_REF] Doglioni | A proposal for kinematic modeling of W-dipping subductions -Possible applications to the Tyrrhenian-Apennines system[END_REF]. Along-strike, the Apennines are divided into northern, central, and southern sectors which are bounded by lithospheric discontinuities trending almost orthogonal to the belt axis [START_REF] Locardi | The origin of the Apennine Arcs[END_REF][START_REF] Ghisetti | Interfering paths of deformation and development of arcs in the foldand-thrust belt of central Apennines (Italy)[END_REF][START_REF] Vai | Basament and early (pre-Alpine) history[END_REF][START_REF] Cavazza | The Mediterranean Area and the Surrounding Regions: Active Processes, Remnants of Former Tethyan Oceans and Related Thrust Belts[END_REF]. From west to east, the now days tectono-stratigraphic units comprising the southern Apennines FTB are [START_REF] Patacca | Geology of southern Apennines[END_REF]: (i) siltstones and claystones of the Liguride/Sicilide oceanic Basin; ii) carbonates derived from the Apennine Platform; iii) mixed terrigenous-carbonate rocks derived from the Lagonegro Basin, which are commonly divided into Lagonegro I and II tectonic units; and iv) carbonates of the Apulian Platform (Fig. 1). During Late Pliocene-Early Pleistocene time, the western and inner portion of the Apulian Platform [START_REF] Mostardini | Appennino centro-meridionale. Sezioni geologiche e proposta di modello strutturale[END_REF][START_REF] Cello | Apennine tectonics in southern Italy: a review[END_REF] was affected by thick-skinned tectonics [START_REF] Butler | Applying thick-skinned tectonic models to the Apennine Accepted Manuscript thrust belt of Italy -Limitations and implications[END_REF][START_REF] Shiner | Thin-skinned versus thick-skinned structural models for Apulian Carbonate Reservoirs: constraints from the Val D'Agri Field[END_REF]. Differently, its outer portion was affected by a significant bulging and development of a Plio-Pleistocene foreland basin system [START_REF] Pieri | Quaternary tectonic activity of the Murge area (Apulian foreland-Southern Italy)[END_REF][START_REF] Borgomano | The Upper Cretaceous carbonates of the Gargano-Murge region, southern Italy: a model of platform-to-basin transition[END_REF][START_REF] Spalluto | Facies evolution and sequence chronostratigraphy of a "mid"-Cretaceous shallowwater carbonate succession of the Apulia Carbonate Platform from the northern Murge area (Apulia, southern Italy)[END_REF][START_REF] Petrullo | Cenozoic tectonic evolution of the northern Apulian carbonate platform (southern Italy)[END_REF].

Monte Alpi Unit

The Monte Alpi Unit is made up of ca. 2000 m-thick, Middle Jurassic to Lower Cretaceous shallowwater carbonates and of 100's of m-thick Messinian carbonate and terrigenous rocks (Fig. 2; De

Accepted Manuscript

Lorenzo, 1895; [START_REF] Selli | Sulla trasgressione del Miocene nell'Italia meridionale[END_REF][START_REF] Sartoni | Ricerche biostratigrafiche nel Mesozoico dell'Appennino Meridionale[END_REF][START_REF] Grandjacquet | Schéma structural de l'Apennin campano-lucanien (Italie)[END_REF][START_REF] Roda | Livelli a struttura grumosa e livelli ad ooliti rotte e rigenerate nel calcare miocenico del Alpi Mt. (Potenza)[END_REF]. The Messinian sedimentary succession is stacked into two intervals [START_REF] Ortolani | Il Mt. Alpi (Lucania) nella paleogeografia dell'Appennino meridionale[END_REF][START_REF] Sgrosso | Nuovi dati biostratigrafici sul Miocene del M. Alpi (Lucania) e conseguenti ipotesi paleogeografiche[END_REF][START_REF] Taddei | Analisi biostratigrafica e considerazioni paleoecologiche sulla successione neogenica del Alpi Mt. (Lucania)[END_REF][START_REF] Van Dijk | Tectonic model and threedimensional fracture network analysis of Alpi Mt. (southern Apennines)[END_REF]. The first one consists of Lower Messinian skeletal carbonates, which stand sub-parallel to the Lower Cretaceous carbonates. The second one is made of Upper Messinian terrigenous deposits, lying with a sharp angular unconformity on both Lower Messinian and Lower Cretaceous carbonates. Although debated in the past, the most recent studies attributed the Mesozoic Monte Alpi carbonates to the Inner Apulian Platform [START_REF] Sgrosso | Nuovi dati biostratigrafici sul Miocene del M. Alpi (Lucania) e conseguenti ipotesi paleogeografiche[END_REF][START_REF] Van Dijk | Tectonic model and threedimensional fracture network analysis of Alpi Mt. (southern Apennines)[END_REF][START_REF] Alberti | New geological data on the basin units surrounding the Monte Alpi unit (southern Italy)[END_REF][START_REF] Mazzoli | Pliocene-Quaternary thrusting, synorogenic extension and tectonic exhumation in the southern Apennines (Italy): Insights from the Alpi Mt. area. In Styles of Continental Contraction[END_REF][START_REF] Bruna | New insights on the structural setting of the Monte Alpi area, Basilicata, Italy[END_REF], 2018). The whole Monte Alpi Unit was interpreted as a push-up structure associated to Quaternary strike-slip tectonics [START_REF] Van Dijk | Tectonic model and threedimensional fracture network analysis of Alpi Mt. (southern Apennines)[END_REF], or as a more complex structure due to combined thin-and thick-skinned Plio-Quaternary compressional tectonics and trans-tensional faulting [START_REF] Shiner | Thin-skinned versus thick-skinned structural models for Apulian Carbonate Reservoirs: constraints from the Val D'Agri Field[END_REF][START_REF] Mazzoli | Pliocene-Quaternary thrusting, synorogenic extension and tectonic exhumation in the southern Apennines (Italy): Insights from the Alpi Mt. area. In Styles of Continental Contraction[END_REF][START_REF] Mazzoli | Low-angle normal faulting and focused exhumation associated with late Pliocene change in tectonic style in the southern Apennines (Italy)[END_REF]. Recently, La [START_REF] Bruna | New insights on the structural setting of the Monte Alpi area, Basilicata, Italy[END_REF] showed that the Monte Alpi structure formed during five deformation stages: 1) foreland bulging and along-foredeep basin stretching, which produced a precompressional, high-angle fault system (pre-Pliocene); 2) emplacement of the allochthon by mean of low-angle thrust faults inducing small-scale strike-slip faults in the Apulian carbonates (Early Pliocene); 3) tectonic inversion of the thrust faults in different levels of the allochthon and onset of low-angle faults (Upper Pliocene); 4) left-lateral, strike-slip motion along NW-SE striking faults and extensional reactivation of pre-existing E-W faults (Lower Pleistocene) followed by left-lateral strikeslip motion of N-S striking faults, and coeval formation of NW-SE striking normal faults (Middle Pleistocene); 5) extension and normal slip on most pre-existing faults which significantly raised and exhumed the Monte Alpi Unit (Middle Pleistocene-Holocene).

Methods

Field analysis

We study two sub-vertical outcrops exposing the Lower Cretaceous limestones. The Solarino and Monte Teduro sites are respectively oriented ca. N-S-and NW-SE, and about 2m 2 in size (Figs. 3a and4a). At each outcrop, detailed stratigraphic logging and qualitative structural analyses aimed at Accepted Manuscript deciphering the nature, attitude, geometry, infill, and abutting/crosscutting relationships of individual fractures are carried out.

Petrographic and mineralogical analyses

The laboratory work includes the petrographic analysis of 60 thin-sections obtained from hand samples collected in the field (29 from the Solarino site, 31 from the Monte Teduro site). The petrographic analysis was carried out using a polarized light Olympus TM microscope BH2, which is equipped with a digital camera Zeiss TM MRc5. Based on their texture the study rocks were sorted according to [START_REF] Dunham | Classification of Carbonate Rocks According to Depositional Textures[END_REF] and [START_REF] Embry | A late Devonian reef tract on northeastern Banks Island, NWT[END_REF] classifications. For mineralogical and cement analysis the thin-sections were examined with the cathodoluminescence technique (Technosyn Cold Cathode Luminescence Model 8200Mk II). We assessed the relative timing of individual diagenetic elements according to superposition and overlap principles [START_REF] Meyers | Carbonate cement stratigraphy of the Lake Valley Formation (Mississippian) Sacramento Mountains, New Mexico[END_REF][START_REF] Goldstein | Practical aspects of cement stratigraphy with illustrations from Pennsylvanian limestone and sandstone, New Mexico and Kansas[END_REF][START_REF] Meyers | Calcite cement stratigraphy; an overview[END_REF][START_REF] Durlet | Séquence diagénétique intrinsèque des surfaces durcies: mise en évidence de surface d'émersion et de leur ablation marine. Exemple de la plate-forme bourguignonne, Bajocien (France)[END_REF][START_REF] Boggs | Petrology of sedimentary rocks[END_REF]. Furthermore, sawing of samples reveals further structural elements invisible at outcrop. Accordingly, the slivers of rock samples obtained during thin section preparation were re-oriented in order to measure the main attitude of the small structural elements visible under the optical microscope.

Results

The Lower Cretaceous carbonates consist of whitish to dark grey limestones arranged in 10's of cm to a few m-thick tabular beds, forming transgressive-regressive depositional depositional sequences dominated by peritidal carbonate facies (Tables 1 and2) and bounded by bedding-parallel surfaces.

The latter appear more prominent than bedding surfaces. Some of them bound a few m-thick bed packages, other bound a few 10's of m-thick beds as documented by Giuffrida et al. (2019b).

Accordingly, these surfaces are named Transgressive Surfaces (TSs) and Prominent Transgressive Surfaces (PTSs), (Figs. 3b,4b,4c,4d,4e). TSs bound a few m-thick depositional sequences and are interpreted as 3 rd order sequence boundaries [START_REF] Spalluto | Facies evolution and sequence chronostratigraphy of a "mid"-Cretaceous shallowwater carbonate succession of the Apulia Carbonate Platform from the northern Murge area (Apulia, southern Italy)[END_REF][START_REF] Rustichelli | Fracture characteristics in Cretaceous platform and ramp carbonates: an outcrop study from Maiella Mountain (central Italy)[END_REF][START_REF] Panza | Fracture stratigraphy and fluid flow properties of shallow-water, tight carbonates: the case study of the Murge Plateau (southern Italy)[END_REF]Giuffrida et al., 2019b). PTSs bound 10's of meters thick depositional sequences and are interpreted as 2 nd order sequence boundaries [START_REF] Spalluto | Facies evolution and sequence chronostratigraphy of a "mid"-Cretaceous shallowwater carbonate succession of the Apulia Carbonate Platform from the northern Murge area (Apulia, southern Italy)[END_REF]Giuffrida et al., 2019b) associated to tectonics and/or global sea level changes [START_REF] Strasser | Depositional sequences in shallow carbonatedominated sedimentary systems: concepts for a high-resolution analysis[END_REF].

Accepted Manuscript

Mesoscale analysis

The two study sites of Solarino and Monte Teduro expose 4 to 60 cm-thick, greyish limestone beds dipping 15° SSE and 30° SE,respectively (Figs. 3c,3d,4c,4d,4e). The high-resolution mapping shows the following fracture sets:

• bed-perpendicular, strata bound joints and sheared joints striking N-S and E-W, and dipping > 70°E and N, respectively (Figs. 3e,3f,3g,4f,4g,4h);

• bed-parallel stylolites (Figs. 3e,3f,3g,4f,4g,4h);

• oblique-to-bedding joints and sheared joints ENE-WSW-striking and ~50° SSE-dipping, (Figs. 3e,3f,3g,4f,4g,4h). In some cases, these oblique-to-bedding structural elements linked bed-perpendicular joints, forming non-strata bound incipient slip surfaces which offset bed interfaces up to a few centimetres ;

• sub-vertical joints and sheared joints striking NNW-SSE, which either crosscut or abut against the sub-horizontal stylolites (Figs. 3e,3f,3g,4f,4g,4h);

• sub-horizontal stylolites, which always abut against the bed-parallel stylolites (Figs. 3e,3f,3g,4f,4g,4h).

Petrographic analysis

Thin-section analysis was key to decipher the carbonate texture originally formed on a flat-topped carbonate platform (Fig. 5, Tables 1 and2). According to their texture, we document a variety of microfacies from wackestones to floatstones and bindstones [START_REF] Dunham | Classification of Carbonate Rocks According to Depositional Textures[END_REF]. Dominant biota and allochems are benthic foraminifera, bivalve bioclasts, ostracods and oncoids. Dasycladacean green algae, gastropods and peloids are less common. Intraformational, oncoid-bearing, angular lithoclasts exclusively occur in Bed 0 (Monte Teduro site), which is bounded by a PTS. Sedimentary and biogenic structures include bed-parallel stromatolitic lamination in microbial bindstones, and fenestral features (original fenestrae-type pores now are filled with blocky calcite). Bioturbations such as burrows and borings occur in Monte Teduro site.

Among the diagenetic products, the microsparry-to-sparry calcite cement is ubiquitous in all microfacies. It is characterized by a dominant blocky texture that destroyed the primary host rock porosity. This frequently patchily distributed cement fills fenestral and bioturbation features, as well

Accepted Manuscript

as the topmost part of geopetal features. Their basal part is filled by a vadose silt. Isopachous calcite cements around grains also occur. Sparse dolomite crystals and recent vuggy pores are rare.

Microstructural analysis

Microstructural analysis revealed the following assemblages:

• Calcite micro-veins ~E-W-striking and ~70°N-dipping, often compartmentalized by fenestral features and/or bioturbation-related bores (Figs. 6a, 6b, 6c, 7a and7b); • cross-orthogonal, bed-perpendicular calcite veins N-S-and E-W-striking, respectively 8b,8c,8d and 9a), cutting across bioturbation-related bores, and abutting against bed-parallel stylolites (Figs. 6a,6b,6c,6d,8a,8b,8c and 8d).

• bed-parallel calcite veins that crosscut bed-perpendicular veins (Figs. 6a,6b,6c,6d,7a,7b,7d,8a,8b,8c,8d,9a,9b and9d); • bed-perpendicular stylolites, which show mutual abutting relationships with the bedparallel veins (Figs. 6a,6b,6c,6d,8a,8b,8c and 8d);

• oblique-to-bedding calcite veins striking ENE-WSW, dipping > 60° SSE, abutting against the bed-perpendicular veins and either crosscutting or terminating against the bed-parallel veins (Figs. 6a,6b,6c,6d,7c,8a,8b,8c,8d,9c and9d); • sub-vertical calcite veins striking NNW-SSE, dipping > 80° WSW, crosscutting all aforementioned structures (Figs. 6a,6b,6c,6d,7d,8a,8b,8c,8d and 9b), and in some cases abutting against the sub-horizontal stylolites (Figs. 6a, 6b, 6c and 6d);

• sub-horizontal calcite veins, which either crosscut or abut against all previous structures (Figs. 6a,6b,6c,6d,7d,7e,8a,8b,8c,8d,9b,9c and 9d), and compartmentalized by high angle-to-bedding stylolites (Figs. 6a, 6b, 6c and 6d);

• sub-vertical calcite veins striking NW-SE, dipping > 85° SW, crosscutting all previous structures (Figs. 8a,8b,8c,8d and 9d).

Data Interpretation

The diagenetic evolution of the Monte Alpi limestones is assessed on petrographic observations under both planar-and cross-polarized lights, coupled with cathodoluminescence analysis of thin sections.

Acording to the principles of [START_REF] Meyers | Carbonate cement stratigraphy of the Lake Valley Formation (Mississippian) Sacramento Mountains, New Mexico[END_REF]1991) our interpretation is proposed as follows.

Diagenetic evolution

Seven diagenetic stages are assessed:

• The Early Calcite Cementation event (EC) is marked by isopachous, non-ferroan, euhedral, limpid calcite cement with crystal sizes between 50 and 400 µm. This cement is characterized by poor luminescence, from black to brown dull. It coats the grains and localizes inside bioturbation bores and on top of the geopets (Figs. 10 and11). This cement is typical of an early diagenetic fabric [START_REF] Choquette | Geologic nomenclature and classification of porosity in sedimentary carbonates[END_REF]. Other evidence for EC occurs in the mud-supported samples where fenestrae and microveins are filled with blocky calcite (Figs. 7a, 7b, 9a and 9b).

• The second stage is marked by the Calcite cement 1 (Cal1). It is a non-ferroan cement made of limpid crystals (Figs. 9a and9b). Under cathodoluminescence, Cal1 cements have a nonluminescent core of 50-200 µm and a light bright-to-orange, luminescent, fringe 5-to-10 µm in size. Cal1 fills the cross-orthogonal, bed-perpendicular veins (Figs. 9a and9b).

• The third stage is characterized by a Calcite cement 2 (Cal2) which consists of a drusy-tomosaic spar that fills bed-parallel veins and some intragranular pores. In planar polarized light, the calcite crystals are subhedral to euhedral, limpid, and 10-to-50 µm in size. In CL, Cal2 comprises two phases Cal2a and Cal2b. Cal2a is non-ferroan, non-luminescent, from black to dull brown calcite (Figs. 7c, 7c1 and7d). Cal2b is made of dull brown ferroan luminescent crystals, bordered by orange-to-bright yellow luminescent fringes (Figs. 7a,7b,7c,7c1,7d,9a,9b,and 9d).

• The fourth stage is associated to the calcite cement 3 (Cal3), which fills the oblique-tobedding veins striking ENE-WSW. It is a limpid, subhedral-to-euhedral, 10-to-200 µm in size calcite (Figs. 7c, 9a and 9d). Crystal cores are mostly ferroan and show a bright orange luminescence under CL (Figs. 7c, 9c and 9d);

Accepted Manuscript

• Stage five is marked by the calcite cement 4 (Cal4) which fills the oblique-to-bedding veins striking NNW-SSE (Figs. 7d and9b). Cal4 is limpid, subhedral and euhedral with sizes ranging between 10 and 50 µm. Under CL, Cal4 is bright brown to bright luminescent (Figs. 7d and9b).

• The sixth stage is associated to the calcite cement 5 (Cal5) which occurs in sub-horizontal veins (Figs. 7d, 9c and 9d). Cal5 is subhedral and euhedral, limpid, ranging from 10 to 50 µm in size. In CL, it is orange-to-yellow bright (Figs 7d, 7e, 9b, 9c and 9d).

• The seventh stage is marked by the calcite cement 6 (Cal6) which occurs in sub-vertical veins striking NW-SE. The ferroan calcite is made of 10-to-100 µm in size, turbid brown and limpid crystals (Figs. 9d). These crystals are dark red-to-orange luminescent under CL, (Figs. 9c and9d).

Structural evolution

In this section, on the basis of the aforementioned diagenetic history, we assessed the time-dependant structural evolution of the study studied limestones by considering both field and laboratory data (Fig. 12):

• The oldest structures are the very tiny E-W veins filled with EC blocky calcite which also filled intragranular pores (J0, Figs. 12a and12b). Some samples bear micro-veins that abut against early fenestral features which were also cemented by EC (Figs. 7a and7b).

• The bed-perpendicular, cross-orthogonal joints and veins (J1) and the bed-parallel stylolites (S1) show mutual abutting relationships (Figs. 12a and12c) are interpreted as coeval [START_REF] Bai | Orthogonal cross joints: do they imply a regional stress rotation[END_REF]. Bed-perpendicular veins crosscut early diagenetic features such as bioturbation and J0 microveins filled with EC blocky calcite. Hence, they J1 postdate J0.

J1 veins are filled with Cal1 characterized by non-luminescent cores, and by bright orange luminescent fringes (Figs. 9a and9b). This evidence denotes a progressive chemical change compared to earliest stage.

• The bed-parallel veins (J2) and bed-perpendicular stylolites (S2) exhibit mutual abutting relationships (Figs. 12a and12d), crosscut both J0 and J1 and are filled with Cal2 cements (Figs. 6b, 6c, 7a, 7b, 7c, 8b, 8c, 9a and 9b). Since Cal2 displays an alternation of dull brown Accepted Manuscript non-luminescent cores (Cal2a, Figs. 7c, 7c1 and 7d) and bright luminescent fringes (Cal2b,Figs. 7a,7b,7c,7c1,7d,9a,9b and 9d), the formation of J2 and S2 is ascribed to telogenesis.

There, oxidizing and reducing conditions likely alternated [START_REF] Richter | Progress in application of cathodoluminescence (CL) in sedimentary petrology[END_REF][START_REF] Boggs | Application of cathodoluminescence imaging to the study of sedimentary rocks[END_REF][START_REF] Hiatt | Cathodoluminescence petrography of carbonate rocks: a review of applications for understanding diagenesis, reservoir quality and pore system evolution[END_REF].

• The oblique-to-bedding veins (J3) abut against J1 (Figs. 3f, 4g, 12a and 12e) and J2 (Figs.

6b, 6c, 7c, 8b, 8c, 9c and 9d) at both meso-and micro-scales. J3 are filled with Cal3 cements which display orange, bright luminescence consistent with reducing conditions [START_REF] Richter | Progress in application of cathodoluminescence (CL) in sedimentary petrology[END_REF]. Accordingly, J3 likely formed during gently increased burial depth with respect to the previous stage.

• Both NNW-SSE-striking oblique-to-bedding joints/veins (J4) and sub-horizontal stylolites (S4) show mutual abutting relationship at the outcrop scale (Figs. 3e,3f,4f,4g,12a and 12f) and crosscut all aforementioned structures at microscale (Figs. 6b,6c,7d,8b,8c and 9c). Since they are filled with Cal5 cements, which are characterized by yellow bright luminescence (Fig. 12), we interpret that J4 formed under reducing conditions [START_REF] Boggs | Application of cathodoluminescence imaging to the study of sedimentary rocks[END_REF] in deep burial diagenetic environments [START_REF] Hiatt | Cathodoluminescence petrography of carbonate rocks: a review of applications for understanding diagenesis, reservoir quality and pore system evolution[END_REF].

• At microscale, sub-horizontal veins (J5) and high-angle to bedding stylolites (S5) show mutual abutting relationships and crosscut all aforementioned structures (Figs. 6b,6c,7d,8b,8c,9c,9d,12a and12g). J5 is filled with Cal5 cements displaying bright orange/yellow luminescence. Therefore, it likely formed under reducing conditions [START_REF] Boggs | Application of cathodoluminescence imaging to the study of sedimentary rocks[END_REF] in burial diagenetic environments [START_REF] Hiatt | Cathodoluminescence petrography of carbonate rocks: a review of applications for understanding diagenesis, reservoir quality and pore system evolution[END_REF].

• The most recent structures are sub-vertical joints and veins (J6). At micro-scale they crosscut all previous structures (Figs. 8b,8c,9d,12a and 12h). They are cemented by Cal6 having bright orange luminescence and, hence, formed under reducing conditions [START_REF] Boggs | Application of cathodoluminescence imaging to the study of sedimentary rocks[END_REF].

Discussion

Micro-to-meso scale structural assemblages

Accepted Manuscript

Both field and laboratory data obtained for the limestones cropping out at the Solarino and Monte Teduro sites are hereafter considered in light of the existing bibliography in order to discuss the deformation mechanisms, geometry and fracture network according to the polyphase tectonic evolution of the Monte Alpi Unit, with a special focus on the modalities of carbonates early embrittlement.

The main structural assemblages deciphered for the study are the following:

(0) Early embrittlement assemblage. The first assemblage is made up by the J0 structural elements, which were strictly related to the EC processes that caused the blocky calcite precipitation in the most fine-grained portions of the sedimentary pile (Fig. 12b). EC occurred during Lower Cretaceous times, when the carbonate sediments experienced shallow marine to meteoric diagenesis (Figs. 13b and13c).

(1) First burial assemblage. It includes both J1 and S1 which formed during Cretaceous times when the burial progressively increased [START_REF] Corrado | Tectonic burial and exhumation in a foreland fold and thrust belt: The Alpi Mt. case history (Southern Apennines, Italy)[END_REF]. Both sets of cross-orthogonal bedperpendicular joint and veins (J1a and J1b) strike E-W and N-S (Figs. 4,6,8 and 13c). They show mutual abutting relationships with respect to the bed-parallel stylolites (La [START_REF] Bruna | New insights on the structural setting of the Monte Alpi area, Basilicata, Italy[END_REF][START_REF] Bruna | Fault growth mechanisms and scaling properties in foreland basin system: The case study of Monte Alpi, Southern Apennines, Italy[END_REF]Giuffrida et al., 2019a). By considering that, J1 sets are filled with Cal1 cements, their sealing occurred under phreatic conditions, when cements contained higher divalent Mn, and low Fe concentrations [START_REF] Boggs | Application of cathodoluminescence imaging to the study of sedimentary rocks[END_REF]. Therefore, we ascribe a burial-related origin for the Cal1 cement (Bathurst, 1975;[START_REF] Tucker | Carbonate sedimentology[END_REF][START_REF] Lavenu | What controls diffuse fractures in platform carbonates? Insights from Provence (France) and Apulia (Italy)[END_REF] occurred during mesogenesis (Figs. 12a and13b) in the sense of [START_REF] Choquette | Geologic nomenclature and classification of porosity in sedimentary carbonates[END_REF].

The coeval formation of cross-orthogonal bed-perpendicular joints induces an asset up under vertical σ1 and horizontal σ2≈σ3 principal stress axes [START_REF] Bai | Fracture spacing in layered rocks: a new explanation based on the stress transition[END_REF][START_REF] Bai | Orthogonal cross joints: do they imply a regional stress rotation[END_REF] during mesogenesis (Figs. 12a,13b and 13c). This brittle mechanism was already documented by [START_REF] Agosta | Architecture and deformation mechanism of a basin bounding normal fault in Mesozoic platform carbonates, central Italy[END_REF], [START_REF] Agosta | From fractures to flow: a field-based quantitative analysis of an outcropping carbonate reservoir[END_REF][START_REF] Agosta | Inner structure and deformation mechanisms of normal faults in conglomerates and carbonate grainstones (Granada Basin, Betic Cordillera, Spain): inferences on fault permeability[END_REF], [START_REF] Rustichelli | Spacing and distribution of bed perpendicular joints throughout layered, shallow-marine carbonates (Granada Basin, southern Spain)[END_REF], 2016[START_REF] Lavenu | Relating background fractures to diagenesis and rock physical properties in a platform-slope transect. Example of the Maiella Mountain (central Italy)[END_REF][START_REF] Lamarche | Facies and Diagenesis Control on Diffuse Fractures in Carbonates[END_REF], and [START_REF] Korneva | Structural properties of fractured and faulted Cretaceous platform carbonates, Murge Plateau (southern Italy)[END_REF] and [START_REF] Panza | Structural architecture and Discrete Fracture Network modelling of layered fractured carbonates (Altamura Fm., Italy)[END_REF][START_REF] Panza | Fracture stratigraphy and fluid flow properties of shallow-water, tight carbonates: the case study of the Murge Plateau (southern Italy)[END_REF] for tight carbonates cropping out in central and southern Italy, and in south-eastern Spain.

(2) Layer Parallel Shortening Assemblage. This assemblage includes bed-parallel veins (J2) and bed-perpendicular stylolites (S2), which formed during Miocene times (Figs. 13b and13c) in

Accepted Manuscript

sub-horizontal limestone beds. Bed-parallel joints were filled with non-ferroan and nonluminescent calcite whose precipitation could be ascribed to the pre-Messinian times during the first telogenesis culmination (Cal2a; figs. 7c, 7c1 and 7d). This structural assemblage was likely associated to the far field propagation of horizontal compressive stresses related to the migrating Southern Apennines FTB thrust front (sensu [START_REF] Geiser | The distribution of layer parallel shortening fabrics in the Appalachian foreland of New York and Pennsylvania: Evidence for two non-coaxial phases of the Alleghanian orogeny[END_REF]. Differently, bed-parallel joints filled with Cal2b calcite, which displays a bright luminescence in CL (Figs.

7a, 7b, 7c, 7c1, 7d, 9a, 9b and 9d), likely formed during Early Messinian in the back-bulge marine deposition zone of the foreland basin system (La [START_REF] Bruna | Fault growth mechanisms and scaling properties in foreland basin system: The case study of Monte Alpi, Southern Apennines, Italy[END_REF]. Quite similar structural assemblage was documented in the Outer Apulian Platform of Italy, both in carbonates platform [START_REF] Graham | Formation and growth of normal faults in carbonates within a compressive environment[END_REF][START_REF] Aydin | Deformation along the leading edge of the Maiella thrust sheet in central Italy[END_REF][START_REF] Rustichelli | Fracture characteristics in Cretaceous platform and ramp carbonates: an outcrop study from Maiella Mountain (central Italy)[END_REF], and ramp [START_REF] Antonellini | Failure modes in deep-water carbonates and their impact for fault development: Majella Mountain, Central Apennines, Italy[END_REF][START_REF] Agosta | Oblique normal faulting along the northern edge of the Majella anticline, central Italy: Inferences on hydrocarbon migration and accumulation[END_REF][START_REF] Agosta | From fractures to flow: a field-based quantitative analysis of an outcropping carbonate reservoir[END_REF][START_REF] Rustichelli | Development and distribution of bedparallel compaction bands and pressure solution seams in carbonates (Bolognano Formation, Majella Mountain, Italy)[END_REF]. However, the present study document for the first time the occurrence of bed-parallel veins in the Apulian carbonates. These structures were described in Jurassic tight limestones of the Lazio-Abruzzi Platform of central Italy by [START_REF] Agosta | Architecture and deformation mechanism of a basin bounding normal fault in Mesozoic platform carbonates, central Italy[END_REF] and [START_REF] Agosta | Geochemical traces of CO2-rich fluid flow along normal faults in central Italy[END_REF], who interpreted them as part of the thrust-assemblage due to transients of high fluid pressure conditions that exceeded the vertical loading (sensu [START_REF] Hubbert | Role of fluid pressure in mechanics of overthrust faulting: I. Mechanics of fluid-filled porous solids and its application to overthrust faulting[END_REF].

(3) Foredeep Basin System Assemblage. This assemblage includes J3 structural elements (Fig. 13c) related to the Late Messinian tectonic evolution of the Monte Alpi foredeep basin, which took place during Late Messinian times synchronous with the deposition of an up to 300 m-thick sedimentary succession [START_REF] Patacca | The Numidian-sand event in the Southern Apennines[END_REF][START_REF] Bruna | Fault growth mechanisms and scaling properties in foreland basin system: The case study of Monte Alpi, Southern Apennines, Italy[END_REF]Figs. 13a and13b). We attribute the J3 formation to localized stress fields due to the shearing of pre-existing structural heterogeneities. Indeed, J3 are envisioned as fault-related structural elements, which cluster at the mode II termination of sheared fracture tip zones, forming splay joints/veins, or at their mode III terminations, forming en-echelon arrays (Figs. 4f and4g). At a larger scale, this structural configuration was documented by Giuffrida et al. (2019b) in nearby outcrops of the Monte Alpi, and by many other authors in the Outer Apulian Platform carbonates of central and southern Italy (ie., [START_REF] Korneva | Characterisation of the permeability anisotropy of Cretaceous platform carbonates by using 3D fracture modeling: the case study of Agri Valley fault zones (southern Italy)[END_REF]Panza et al., 2018, and references therein).

Accepted Manuscript

(4) Tectonic burial assemblage. During Early Pliocene, the tectonic load related to the juxtaposition of the Southern Apennines FTB onto the Apulian carbonates [START_REF] Cello | Apennine tectonics in southern Italy: a review[END_REF][START_REF] Patacca | Geology of southern Apennines[END_REF][START_REF] Tavani | A review of deformation pattern templates in foreland basin systems and fold-and-thrust belts: Implications for the state of stress in the frontal regions of thrust wedges[END_REF] led to the formation of J4 and S4 structures. Hence, they are interpreted as due to a second burial event of the Monte Alpi carbonates (Figs. 13a to 13c). Since coeval Cal4 cements display bright brown to bright yellow luminescent colours (Figs. 7d and9b), we assess that the precipitation took place under reducing conditions at depths of 5-6 km [START_REF] Corrado | Tectonic burial and exhumation in a foreland fold and thrust belt: The Alpi Mt. case history (Southern Apennines, Italy)[END_REF][START_REF] Mazzoli | Pliocene-Quaternary thrusting, synorogenic extension and tectonic exhumation in the southern Apennines (Italy): Insights from the Alpi Mt. area. In Styles of Continental Contraction[END_REF].

(5) Deep-seated thrusting assemblage. During Late Pliocene times, S5 and J5 structures formed when deep-seated reverse faulting affected the Monte Alpi Unit [START_REF] Shiner | Thin-skinned versus thick-skinned structural models for Apulian Carbonate Reservoirs: constraints from the Val D'Agri Field[END_REF][START_REF] Mazzoli | Pliocene-Quaternary thrusting, synorogenic extension and tectonic exhumation in the southern Apennines (Italy): Insights from the Alpi Mt. area. In Styles of Continental Contraction[END_REF]Mazzoli et al., 2008) (Figs. 13a to 13c). Deep burial conditions are inferred and supported by the bright orange luminescence of J5 micro-veins (Figs. 7e, 9b, 9c and9d). We therefore document the aforementioned structural elements in the Apulian carbonates, whereas their occurrence was previously assessed by [START_REF] Agosta | Architecture and deformation mechanism of a basin bounding normal fault in Mesozoic platform carbonates, central Italy[END_REF] for the Jurassic limestones of Lazio-Abruzzi carbonate Platform exposed in central Italy.

(6) Polyphase transpressional/extensional exhumation assemblage. The last assemblage includes J6 that formed during the latest tectonic stages [START_REF] Mazzoli | Low-angle normal faulting and focused exhumation associated with late Pliocene change in tectonic style in the southern Apennines (Italy)[END_REF][START_REF] Bruna | New insights on the structural setting of the Monte Alpi area, Basilicata, Italy[END_REF], 2018;) which crosscut all previous assemblages (Figs. 9c and9d) and were dilated during exhumation form depth (Figs. 13a to 13c). Similar structures were documented throughout the whole Outer Apulian Platform exposed in central and southern Italy [START_REF] Korneva | Structural properties of fractured and faulted Cretaceous platform carbonates, Murge Plateau (southern Italy)[END_REF][START_REF] Panza | Fracture stratigraphy and fluid flow properties of shallow-water, tight carbonates: the case study of the Murge Plateau (southern Italy)[END_REF].

Early structural diagenesis

We know that platform carbonates are commonly affected by early diagenetic modifications [START_REF] Anselmetti | Controls on sonic velocity in carbonates[END_REF] which may increase their stiffness in case of Early Cementation, EC [START_REF] Eberli | Factors controlling elastic properties in carbonate sediments and rocks[END_REF]. In the Monte Alpi Unit, we documented that in carbonate mudstones early cements filled pores associated to either bioturbation or to fenestral porosity (Figs. 10 and11). The carbonate mud intervals were originally deposited in a back-reef inner platform/platform margin setting (cf. Figs. 9a and9b), and were affected by a EC processes that took place at the water-sediment interface or at very shallow depth enhanced by micro-organisms on living organisms and calcite grains Accepted Manuscript (Bathurst 1975). These micro-organisms perforated the calcitic envelope of the original grains, and triggered micritization at the onset of eogenesis [START_REF] Tucker | Carbonate sedimentology[END_REF]).

In the mud-supported lithified sediments, early embrittlement took place prior to bioturbation (boring) of hard substrates (cf. thin sections T0Bb, T6a, T7b, and T8d, Table 2, and Fig. 5d).

Accordingly, we envision that both dissolution cavities (vuggy porosity sensu [START_REF] Choquette | Geologic nomenclature and classification of porosity in sedimentary carbonates[END_REF] and blocky cements formed during transients of platform emersions. They were therefore, subjected to meteoric diagenesis, then partially obliterated by the bores during the subsequent marine transgressions. Hence, EC processes led to rapid lithification and embrittlement of selective portions of the carbonate pile, which was affected by localized brittle failure and pressure solution [START_REF] Nelson | Significance of fracture sets associated with stylolite zones: geologic notes[END_REF][START_REF] Nelson | Geologic analysis of naturally fractured reservoirs[END_REF][START_REF] Wennberg | Fracture intensity vs. mechanical stratigraphy in platform top carbonates: the Aquitanian of the Asmari Formation, Khaviz Anticline, Zagros, SW Iran[END_REF][START_REF] Rustichelli | Development and distribution of bedparallel compaction bands and pressure solution seams in carbonates (Bolognano Formation, Majella Mountain, Italy)[END_REF][START_REF] Rustichelli | Spacing and distribution of bed perpendicular joints throughout layered, shallow-marine carbonates (Granada Basin, southern Spain)[END_REF][START_REF] Rustichelli | Bedding-parallel stylolites in shallow-water limestone successions of the Apulian Carbonate Platform (central-southern Italy)[END_REF][START_REF] Lavenu | Background fractures in carbonates: inference on control of sedimentary facies, diagenesis and petrophysics on rock mechanical behavior. Example of the Murge Plateau (southern Italy)[END_REF][START_REF] Lavenu | What controls diffuse fractures in platform carbonates? Insights from Provence (France) and Apulia (Italy)[END_REF].

These results show that the subsequent mechanical behaviour of the studied limestones is also related to their very early diagenetic evolution, which controlled the initial lithification of the carbonate muds.

Conclusions

The present study combined field and laboratory analyses to reconstruct the nature and timing of fracture networks in Lower Cretaceous limestones exposed at the Monte Alpi, southern Italy. We first deciphered both diagenetic and structural evolution of the limestones, and then proposed a conceptual model related to the time-dependant evolution of the structural assemblages in light of the complex tectonic history of the southern Apennines. We focussed on the early cementation processes responsible for the onset of joints and veins at very shallow burial conditions. These processes played a fundamental role on subsequent development of the present-day mechanical and fracture stratigraphy. Specifically, we assessed the following assemblages: (0) early embrittlement assemblage (Lower Cretaceous) ascribed to a first stage of eogenesis characterized by early calcite cementation processes and fracture development in the mudrich portions of the carbonate pile;

(1) first burial assemblage (Cretaceous) related to the growth of the Inner Apulian Platform and the progressive burial which caused the formation of bed-parallel stylolites and two sets of cross-orthogonal bed-perpendicular joints and veins;

Accepted Manuscript

(2) layer parallel shortening assemblage (pre-Messinian) due to the FTB far field stress propagation within the Inner Apulian Platform, and characterised by one set of bedperpendicular stylolites and bed-parallel veins;

(3) foredeep basin system assemblage (Late Messinian) related to fault activity during the structural evolution of the Monte Alpi foreland basin system, and composed of NW-SE striking joints and veins;

(4) tectonic burial assemblage (Early Pliocene) due to the tectonic loading of the southern Apennines allochthon and made up of oblique-to-bedding joint, veins and stylolites.

(5) deep-seated thrusting assemblage (Late Pliocene) due to steep reverse faults, and made up of sub-vertical stylolites and low-angle joints and veins;

(6) polyphase transpressional/extensional exhumation assemblage (Early Pleistocene to Holocene) related to strike-slip faulting and the latest rock exhumation. It comprises subvertical joints and veins that crosscut all previous structural assemblages.

We assessed that early calcite (EC) precipitation mainly occurred within mud-rich carbonate sediments. Both pore dimensions and texture variations were factors driving EC processes in carbonates. We concluded that localized early embrittlement of carbonates determined the subsequent early fractures nucleation in mudstones beds and provided new insights into the mechanical control and nucleation of diffuse fractures. Therefore, these diffuse fractures providing the background permeability in naturally fractured carbonate reservoirs are due to early burial diagenesis that cause the stiffening of the finer grained portions of the carbonate pile.

Vitale, S., Dati, F., Mazzoli, S., Ciarcia, S., Guerriero, V., Iannace, A., 2012. Modes and timing of fracture network development in poly-deformed carbonate reservoir analogues, Mt. Chianello, southern Italy. Journal of Structural Geology, 37, 223-235. Vitale, S., Ciarcia, S., 2013. Tectono-stratigraphic and kinematic evolution of the southern Apennines/Calabria-Peloritani Terrane system (Italy). Tectonophysics, 583, 164-182. [START_REF] Bonardi | [END_REF][START_REF] Cosentino | Evoluzione cinematica del sistema orogenico dell'Appennino centro-meridionale: caratterizzazione stratigrafico-strutturale dei bacini sintettonici[END_REF][START_REF] Patacca | Geology of southern Apennines[END_REF]Vitale and Ciarcia, 2013,) and NE-SW geological cross-section modified after Mazzoli et al., 2008. (b) Sketch map of part of the southern Apennines showing the study area.

Figure captions

Accepted Manuscript

Fig. 1 .

 1 Fig.1. (a) Simplified geological map of Southern Apennines, Italy (from[START_REF] Bonardi | [END_REF][START_REF] Cosentino | Evoluzione cinematica del sistema orogenico dell'Appennino centro-meridionale: caratterizzazione stratigrafico-strutturale dei bacini sintettonici[END_REF]

Fig. 2 .

 2 Fig.2. Geological map of Monte Alpi, (Basilicata, Italy; modified after La Bruna et al., 2017) with location of the studied sites.

Fig. 3 .

 3 Fig.3. (a) Panoramic overview of the western edge of Monte Alpi; (b) focus on the southern portion of the western cliff; (c) stratigraphic log; (d) outcrop view of the studied Solarino site; (e) close up view of the studied outcrop; (f) line drawing of the studied outcrop; (g) lower hemisphere equal area projection of the structures presented in e.

Fig. 4 .

 4 Fig.4. (a) Close up view of the southern portion of the western cliff; (b) panoramic overview of the Monte Teduro cliff; (c) close up of a portion of the studied Monte Teduro cliff; (d) stratigraphic log; (e) view of the studied outcrop; (f) close up of the outcrop; (g) line drawing map of the studied outcrop;(h) lower hemisphere equal area projection of the structures presented in g.

Fig. 5 .

 5 Fig.5. (a to d) Photomicrographs (cross-polarized light) of representative microfacies of the Lower Cretaceous platform carbonates.

Fig. 6 .

 6 Fig.6. Solarino site, (a) Scanned thin-section; (b) line drawing of the scanned thin-section; (c) cartoon of the structural assemblage presented in b; (d) lower hemisphere equal area projection as poles of the structures that are presented in b and c.

Fig. 7 .

 7 Fig.7. Thin-section zooms a to e: planar-polarized light and cathodoluminescence microphotographsshowing the main characteristics and chronologies of fractures and cements. See text for explanation.

Fig. 8 .Fig. 9 .

 89 Fig.8. Teduro site, (a) Scanned thin section; (b) line drawing of the scanned thin section; (c) cartoon of the structural assemblage documented in b; (d) lower hemisphere equal area projection as poles of the structures presented in b and c.

Fig. 10 .

 10 Fig.10. Scanned image of a Lithoclastic-oncolitic floatstone. Plane-polarized light and cathodoluminescence photomicrographs (zoom 1) display early calcite cement localized within bores.Bores formed after blocky cement which filled previous cavities. Cavities are related to a platform emersion phase, differently bores formed during subsequent marine transgression and were filled with early calcite cement (ec).

Fig. 11 .Fig. 12 .

 1112 Fig.11. Scanned image of Fenestral microbial bindstone. Early calcite cement filled geopetal structures. Plane-polarized and cathodoluminescence photomicrographs (zoom 1 and 2) display large patches of blocky calcite cement and geopetal early features which represent a typical early diagenetic fabric.

Fig. 13 .

 13 Fig.13. Time/space evolution model proposed for Monte Alpi. (a) main tectonic steps from the pre-Messinian to the Holocene time (after La Bruna et al, 2017-2018); (b) burial history of the Monte AlpiApulian carbonates associated to the main tectonic events presented in a (modified after[START_REF] Mazzoli | Pliocene-Quaternary thrusting, synorogenic extension and tectonic exhumation in the southern Apennines (Italy): Insights from the Alpi Mt. area. In Styles of Continental Contraction[END_REF]; (c) idealized block diagrams showing the overall structural assemblages observed at meso and microscale.

  Fig.7e

  Fig. 9c

  Fig. 9d

Acknowledgments

VLB acknowledges Giacomo Prosser, Anthony Tendil, and Paola Castelluccio for the support provided during field and laboratory analyses, and Christophe Matonti for the interesting and useful discussion on timing of structural diagenesis. The detailed revision provided by Dr. Arthur Lavenu and by an anonymous reviewer sensitively improved the quality of the manuscript. This work was co-financed by the Vinci Program (Université Franco-Italienne), and by the Reservoir Characterization Project (www.rechproject.com).

Accepted Manuscript