Unravelling the Tectonic Evolution of the Dinarides – Alps – Pannonian Basin Transition Zone: Insights from Structural Analysis and Low-Temperature Thermochronology from Ivanščica Mt., NW Croatia

Unravelling the Tectonic Evolution of the Dinarides – Alps – Pannonian Basin Transition Zone: Insights from Structural Analysis and Low-Temperature Thermochronology from Ivanščica Mt., NW Croatia | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article Unravelling the Tectonic Evolution of the Dinarides – Alps – Pannonian Basin Transition Zone: Insights from Structural Analysis and Low-Temperature Thermochronology from Ivanščica Mt., NW Croatia Matija Vukovski, Marko Špelić, Duje Kukoč, Tamara Troskot-Čorbić, and 3 more This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-3991799/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 02 Sep, 2024 Read the published version in Swiss Journal of Geosciences → Version 1 posted 7 You are reading this latest preprint version Abstract A comprehensive study, including geological mapping, structural and thermochronological analysis, has been carried out on Ivanščica Mountain (NW Croatia), with the aim to contribute in reconstruction of the tectonic history of the Dinarides, Southern/Eastern Alps and Pannonian Basin transitional zone. Implementation of structural and thermochronological methods enabled a subdivision of Ivanščica Mt. into three structural domains (from bottom to top): Ivanščica Parautochton, Ivanščica Imbricates and Oligo-Neogene sedimentary cover. In addition, a sequence of deformational events in tectonic history of this transitional zone is proposed, comprising three extensional and four contractional events starting from Middle Triassic until present times. Oldest deformational events indicating Middle Triassic (D1) and Early Jurassic (D2) extensional phases were recognised only in volcano-sedimentary record. The oldest contractional event (D3) is related to obduction of the Neotethyan ophiolitic mélange over Upper Triassic to Lower Cretaceous succession of the eastern margin of the Adriatic microplate, which resulted in thermal alteration of the Ivanščica Imbricates structural domain in Berriasian - Valanginian times (~ 140 Ma). This event was soon followed by another contractional event (D4), which resulted in thrusting and imbrication of the Adriatic passive margin successions together with tectonically emplaced ophiolitic mélange, thermal alteration of the footwall successions, fast exhumation and erosion. Apatite fission track data together with syn-tectonic deposits indicate Hauterivian to Albian age of this event (~ 133–100 Ma). These Mesozoic structures were rotated in post-Oligocene times and brought from initially typically Dinaridic SE striking and SW verging structures to recent SW striking and NW verging structures. Following extensional event (D5) manifested in the formation of SE striking and mostly NE dipping normal listric faults, and ENE striking dextral faults accommodating top-NE extension in the Pannonian Basin. Deformations were coupled with hanging wall sedimentation of Ottnangian to middle Badenian (~ 18–14 Ma) syn-rift deposit as observed from the reflection seismic and well data. Short lasting contraction (D6) was registered in the late Sarmatian (~ 12 Ma). The youngest documented deformational event (D7) resulted in reactivation of ENE striking dextral faults, formation of SE striking dextral faults as well as the formation of E to NE trending folds and reverse faults. This event corresponds to Late Pannonian (~ 6 Ma) to recent NNW-SSE contraction driven by the indentation and counterclockwise rotation of Adriatic microplate. Recognized tectonic events and their timings indicate that Ivanščica was mainly affected by deformational phases related to the Mesozoic evolution of the Neotethys Ocean as well as Cenozoic opening and inversion of the Pannonian Basin. Mesozoic tectono-sedimentary evolution of Ivanščica Mountain exhibits clear Dinaridic affiliation, more precisely, that of the Pre-Karst zone of the Dinarides. Northern Neotethys Adriatic passive margin ophiolite obduction nappe stacking imbricate fan structural inheritance tectonic inversion Pre-Karst zone Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Figure 10 Figure 11 1. Introduction Synchronous mountain building of neighbouring orogens often results with their complex structural architectures and overprinting relationships. Such complex relationships can only be resolved by comprehensive studies that integrate lithostratigraphic, structural and thermochronological data obtained at local to regional scales of observations. In particular, such approach is inevitable in cases when both orogens are affected by post-orogenic extensional tectonics, a geodynamic scenario known from the past and at present in almost all peri-Mediterranean orogens (e.g., Meulenkamp et al., 1988 ; Jolivet & Faccenna, 2000 ; Faccenna et al., 2004 , 2013 ; Kissling et al., 2006 ). This scenario, which commonly includes post-orogenic local- to regional-scale translations and rotations of differently sized tectonic blocks dismembered from previously formed collisional nappe stacks, is also known from the Dinarides – Alps – Pannonian Basin transitional zone (Fig. 1 ; e.g., Placer, 1999a ; Haas et al., 2000 ; Tomljenović et al., 2008 ; van Gelder et al., 2015 ). Namely, this area records complex tectonic histories in the orogenic build-up of the Southern-Eastern Alps and the Dinarides, followed by several phases of extension and contraction in the tectonic evolution of the SW margin of the Pannonian Basin (e.g., Fodor et al., 1998 ; Vrabec & Fodor, 2006; Tomljenović & Csontos, 2001 ; van Gelder et al., 2015 ; Fodor et al., 2021 ). Here, Mesozoic formations of both orogens preserve records of geodynamic processes that resulted with opening and closure of the northern branch of the Neotethys Ocean (e.g., Pamić et al., 1998 ; Pamić, 2002 ; Schmid et al., 2008 ; 2020 ; Ustaszewski et al., 2010 ; the Balkan Neotethys sensu van Hinsbergen et al., 2020 ). In addition, the Alps record another, younger collisional event related to the closure of the Alpine Tethys Ocean (e.g., Neubauer et al., 1999 ; Willingshofer et al., 1999a ; Schmid et al., 2008 ; 2020 ; van Hinsbergen et al., 2020 ). Both oceanic realms contemporaneously existed during a part of Mesozoic times, separating the Adria microplate and the Eurasia (e.g., van Hinsbergen et al., 2020 ). However, during the time of their closure, which differs for each of these oceanic realms, the Adriatic microplate was in a different tectonic position with respect to the European plate: lower plate in the Dinarides, and the upper plate in the Alps (e.g., Doglioni et al., 1999 ; Schmid et al., 2008 , 2020 ). Due to the complex Mesozoic and Cenozoic geodynamics at the Dinarides-Southern/Eastern Alps-Pannonian Basin transitional zone (Fig. 1 a, b), a detail reconstruction of tectonic and depositional history, in its part in the northern Croatia, is still little known. Among several inselbergs in this area (Fig. 1 c), Medvednica Mt. is the most comprehensively studied so far, providing a large data set on different topics in Mesozoic stratigraphy (e.g., Halamić et al., 1999, 2005 ; Babić et al., 2002 , with references therein), metamorphic and igneous petrology (e.g., Belak & Tibljaš, 1998 ; Slovenec & Pamić, 2002 ; Lugović et al., 2007 ; Judik et al., 2008 ; Belak et al., 2022 ; Mišur et al., 2023 ;), paleomagnetism, structural architecture and tectonics (e.g., Tomljenović et al., 2008 ; van Gelder et al., 2015 ). Results of most of these studies, in combination with data from the Basic Geological Map of Yugoslavia, sheet Rogatec (Aničić & Juriša, 1984 ) and sheet Varaždin (Šimunić et al., 1982 ), were so far used in correlation of pre-Neogene tectonic units of this transitional zone with corresponding tectonic units differentiated within much wider area (e.g., Haas et al., 2000 ; van Gelder et al., 2015 ) and across the Alpine-Carpathian-Dinaridic-Hellenic orogenic system (e.g., Schmid et al., 2008 , 2020 ; van Hinsbergen et al., 2020 ). Compared with the neighbouring Medvednica Mt., modern data on geology of the Ivanščica Mt. were relatively scarce (Babić et al., 2002 ; Goričan et al. 2005 ; Lužar-Oberiter et al., 2009 , 2012 ), until a series of recently published studies released by the GOST project ( https://projectgost.wordpress.com ). These studies provide new data set on stratigraphy (Slovenec et al. 2020 ; Kukoč et al., 2023 , 2024 ), petrology (Slovenec & Šegvić, 2024 ; Slovenec et al., 2023 ; Šegvić et al., 2022) and lithostratigraphy of the Adriatic passive margin successions (Vukovski et al., 2023 ) tectonically assembled into the structural architecture of this mountain. As a supplement to published studies of the GOST project, this paper aims to present new and more detailed data on spatial arrangement, kinematics and age of deformational structures in Mesozoic and Cenozoic rocks of Ivanščica Mt. and its neighbouring area. These data are obtained by a multi-scale structural analysis, including geological mapping, interpretation of reflection seismic sections, vitrinite reflectance and apatite fission track methods. After a short overview on geological and structural settings of Ivanščica Mt. based on previously published data, this paper presents new data on structural architecture and low-temperature thermochronology of the study area. These data are then used to propose a sequence of deformational events in the study area, which is correlated with deformational sequences revealed in neighbouring areas of Dinarides and Southern-Eastern Alps, all together discussed in the context of tectonic evolution of the Dinarides, Southern-Eastern Alps and the SW margin of the Pannonian Basin, starting from the Middle Triassic until present. Finally, we propose a new correlation between distinguished tectonic units of Ivanščica Mt. with those known from the Internal Dinarides. 2. Geological setting of Ivanščica Mountain 2.1. Lithostratigraphic characteristics Ivanščica Mt. is built of Upper Paleozoic and Mesozoic sedimentary successions originating from the passive margin of the Adria microplate and its basement, the Neotethyan ophiolitic mélange and Oligocene-Quaternary sedimentary cover of the Pannonian Basin (Fig. 2 ; Šimunić et al., 1982 ; Aničić & Juriša 1984 ). The oldest rocks on Ivanščica Mt. are Permian brown-red conglomerates, sandstones and black shales concordantly overlain by Lower Triassic clastic deposits, including sporadic1-2 m thick dolomite layer along the contact (Šimunić et al., 1982 ; Šimunić & Šimunić, 1997 ). Lower Triassic sediments consist of micaceous sandstones, mica siltstones, shale and marls in the lower part and dark-grey, tabular, thin-bedded limestones in the upper part (Šimunić & Šimunić, 1997 ). Paleozoic and Lower Triassic deposits have spatially limited exposure on the northern slopes of the mountain. These deposits originated from a shallow-marine environment (Šimunić et al., 1982 ). The largest part of the mountain is built of several hundred meters thick Middle Triassic deposits, predominantly shallow-marine dolomites and limestones (Šimunić et al., 1982 ). Pelagic successions consisting of Anisian to Ladinian pelagic limestone and radiolarian chert intercalated with volcanic and volcaniclastic lithologies ranging from basic to acidic are also present (Goričan et al., 2005 ; Slovenec et al., 2020 , 2023 ; Kukoč et al., 2023 ; Smirčić et al., 2024 ). These pelagic successions are several tens of meters thick, generally tectonically disturbed and their contacts with the underlying and overlying formations are rarely exposed. Middle Triassic successions reflect a period of intense tectonic activity related to the opening of the Neotethys Ocean and the formation of a horst-and-graben depositional environments as a result of extension (Goričan et al., 2005 ; Kukoč et al., 2023 ). Deep-marine basins formed during this period were relatively short-lived and carbonate platform sedimentation was reestablished in the late Ladinian (Goričan et al., 2005 ). Upper Triassic sediments of Ivanščica Mt. are exclusively shallow-marine and consist of several hundred meters thick series of dolomites and limestones (Šimunić et al., 1982 ; Šimunić & Šimunić, 1997 ). These are the equivalent of the Main Dolomite and Dachstein Limestone found in the Alps (Vukovski et al., 2023 ). Lower Jurassic to Lower Cretaceous deposits are exposed in the central part of Ivanščica Mt. Successions composed of these deposits differ in the southern and northern parts of central Ivanščica. In the northern part, shallow-marine Lower Jurassic limestone conformably overlie Upper Triassic carbonates and are in turn overlain by Middle Jurassic pelagic limestone (Vukovski et al., 2023 ). In the southern part, Upper Triassic deposits are overlain by Lower Jurassic thick pelagic series consisting of pelagic limestone, carbonate breccia, marl and calcarenites (Babić, 1974 ; Vukovski et al., 2023 ). Middle to Late Jurassic radiolarian cherts are recorded in both areas, however, their contact with underling deposits and complete thickness is not known. In both areas, radiolarian cherts conformably pass up-section into Tithonian to Valanginian pelagic Aptychus limestone with several beds of calcarenites sporadically occurring at the contact as recorded in the southern part of central Ivanščica (Babić & Zupanič, 1973 ; Vukovski et al., 2023 ). The youngest Mesozoic deposits are mixed carbonate-siliciclastic turbidites of the Hauterivian to Albian Oštrc Formation (Zupanič et al., 1981 ; Lužar-Oberiter et al., 2009 , 2012 ), which overly the Aptychus limestone. Upper Triassic to Lower Cretaceous sedimentary successions of Ivanščica Mt. are interpreted as deposited on the eastern passive margin of the Adria microplate, which was facing the evolving Neotethys Ocean from the Middle Triassic until the ophiolite obduction in latest Jurassic-earliest Cretaceous (Schmid et al., 2008 , 2020 ). Sedimentation on this margin reflected regional tectonic activity as well as changes in ocean fertility during this period. Resedimented shallow-marine material was likely supplied from the adjacent Adriatic Carbonate Platform (Vukovski et al., 2023 ). The turbidites of the Oštrc Fm. have been interpreted as deposited in a clastic wedge in front of the advancing nappes carrying the Neotethys ophiolites (Lužar-Oberiter et al., 2009 , 2012 ). On the southern slopes of Ivanščica Mt., in its central and eastern parts, an ophiolitic mélange is widely exposed, named as the Repno complex (Babić & Zupanič, 1978 ; Babić et al., 2002 ) (Fig. 2 ). This ophiolitic mélange is composed of centimeter to hundred meters sized blocks of sandstone, chert, basalt and gabbro chaotically embedded within a shaly-silty matrix (Babić et al., 2002 ; Slovenec et al., 2011 ; Kukoč et al., 2024 ). It is interpreted as formed during the Middle Jurassic supra-subduction in the northern branch of Neotethys Ocean and subsequent Late Jurassic to earliest Cretaceous obduction of ophiolites of this oceanic realm on the eastern Adriatic margin (Babić et al., 2002 ; Kukoč et al., 2024 ). The oldest Cenozoic deposits on Ivanščica Mt. comprise around 350 m thick Late Egerian clastic deposits with coal seams (Šimunić et al., 1982 ; Fig. 2 ). These deposits lay unconformably over different Mesozoic formations on the southern slopes of the mountain, or locally in tectonic contact with underlying Mesozoic formations (Fig. 2 ). On the northern slopes, Upper Oligocene to Lower Miocene predominantly clastic deposits with marls, clays and tuffs are found in tectonic contact and dip underneath the Mesozoic formations (Fig. 2 ). This around two kilometers thick Upper Oligocene – Lower Miocene succession is interpreted as deposited within the Hrvatsko Zagorje Basin, a marginal basin of the Central Paratethys Sea (Avanić et al., 2021 ). Its southern margin is interpreted as located along the present-day southern slopes of Ivanščica Mt. (Pavelić & Kovačić, 2018 ). Further to the south, a separate Neogene basin, named the North Croatian Basin, formed since the late Early Miocene (Pavelić, 2002 ; Pavelić & Kovačić, 2018 ). Deposition of Ottnangian to middle Badenian alluvial to marine succession with volcaniclastics marks the syn-rift period of the basin evolution. Further deepening of the depositional environment resulted in unification of both basins and widespread sedimentation of predominantly marls and limestones during middle Badenian (Pavelić & Kovačić, 2018 ). Regional Late Badenian transgression and cassation of volcanic activity mark the end of the rifting stage and the onset of post-rift thermal subsidence (Pavelić & Kovačić, 2018 ). Sarmatian and Early Pannonian were characterized by the deposition of marine to brackish marls and limestones. During the Late Miocene and Pliocene, the brackish lake was continuously infilled by the turbiditic, deltaic, and finally alluvial clastic sequence (Pavelić & Kovačić et al., 2018). These were overlain by Quaternary clastic deposits (Šimunić et al., 1982 ). 2.2. Structural characteristics Structurally, Ivanščica Mt., together with the other mountains of northern Croatia, is considered as an eastern continuation of the Sava folds (Šimunić et al. 1979, 1982 ; Šimunić 1992 ; Fig. 1 c), a tectonic unit first described by Winkler ( 1923 ) and later by Placer ( 1999b ). During their work on the Basic geological map of SFRY, sheet Varaždin, Šimunić et al. (1979, 1982 ) considered all mapped faults on Ivanščica to be of Cenozoic age, with the main contractional deformations occurring during the Miocene. These authors interpreted Ivanščica as a N-vergent nappe, which brought Paleozoic and Mesozoic formations over Oligocene and earliest Miocene sediments during Early Miocene (in Eggenburgian). The occurrences of Triassic-Jurassic carbonates in the southern part of central Ivanščica were interpreted as erosional remains of structurally higher nappe (Šimunić et al., 1979, 1982 ) or as olistoliths embedded in the Repno complex (Babić & Zupanič, 1978 ). As we will show below, we interpret those occurrences as a stack of imbricates built of passive margin successions and the Repno complex, formed during an Early Cretaceous contractional event. More recent studies consider northern Croatian mountains, including Ivanščica Mt., to be a part of the Southern Alps unit (Placer, 1999a ). According to van Gelder et al. ( 2015 ) and Schmid et al. ( 2008 , 2020 ), Ivanščica exposes a part of S-vergent South Alpine nappe emplaced over the Internal Dinaridic units during Miocene times. Prior to this emplacement, the tectonic block carrying northern Croatian mountains undergone Oligocene–earliest Miocene 130° clockwise rotation, as interpreted by Tomljenović et al. ( 2008 ) based on paleomagnetic data measured in Upper Cretaceous deposits on Medvednica Mt. Subsequent normal faulting related to Early Miocene rifting and opening of this part of the Pannonian Basin overprinted older structures (Tomljenović & Csontos, 2001 ; van Gelder et al., 2015 ). Basin inversion, which initiated in Late Miocene-Pliocene, caused folding and reverse faulting resulting in the final uplift of the north Croatian mountains (Tomljenović & Csontos, 2001 ). This inversion was coeval with approximately 35° counterclockwise (CCW) rotation, active in Miocene to recent times, presumed as driven by the CCW rotation and indentation of the Adriatic microplate (Tomljenović & Csontos, 2001 ; Márton et al., 2002 ). 3. Methods and Results 3.1. Description of deformational structures Ivanščica is a densely forested mountain with rather scarce high-quality geological outcrops. For this reason, extensive fieldwork was carried out. At locations considered as essential for better understanding of deformational history of study area, detail geological mapping in scales 1:25 000 and 1:5 000 was conducted. Special attention was given to the collection of data on deformation structures and kinematic data. Acquired data include measurements of orientation of bedding, meso-scale folds, axial plane cleavage, S-C fabrics, intersection lineations, fault planes and their kinematics, many of these recorded for the first time. Based on measured structural data, observed differences in deformation styles and mapped tectonic and depositional contacts shown in maps (Figs. 2 , 3 ) and cross-sections (Fig. 4 ), the study area is subdivided into three structural domains that from bottom to top are: Structural domain Ivanščica parautochton (SDIP), Structural domain Ivanščica imbricates (SDII) and Structural domain Oligo-Neogene sedimentary cover (SDONC). 3.1.1. Structural domain Ivanščica Parautochton (SDIP) Structural domain Ivanščica Parautochton (SDIP) comprises Permo-Mesozoic formations exposed along its northern slopes (Figs. 2 , 4 ). This domain is cut and broken apart into two structural blocks to the west and east of the SE striking Gotalovec – Prigorec dextral fault (Fig. 2 ). In both structural blocks, this structural domain is overthrust by the SDII along the SE-dipping Črne Mlake roof thrust (ČMT; Figs. 2 , 4 ). On its SW margin, the SDIP is unconformably overlain by Oligo–Neogene sediments. However, in part of mountain SW of the Vilinska špica peak (726 m), Middle Triassic formations of the SDIP are brought over Oligocene deposits by two NNW-dipping reverse faults, with only locally preserved original depositional contact (Fig. 2 ). Contrary, no original depositional contacts between Oligo-Neogene cover and Permo-Mesozoic formations of the SDIP are preserved in the northern slopes of Ivanščica Mt. Here, Permo-Mesozoic formations of the SDIP are thrusted northward over Oligo-Neogene sediments (Figs. 2 , 4 ). In the central part of the mountain, the complete and tectonically nearly undisturbed Permo-Mesozoic succession is homoclinally dipping towards S to SE below the SDII and the Oligo–Neogene cover (Fig. 4 ). This homoclinal structure of the SDIP is thrusted towards NW over the rest of Permo-Mesozoic units belonging to the same structural domain (Figs. 2 , 4 ). These footwall units are arranged in a several SE-dipping imbricates and thrusted NW-ward over uppermost Oligocene to Lower Miocene sediments (Figs. 2 , 4 ). The youngest strata in this homocline are Lower Cretaceous turbidites of the Oštrc Fm. representing the highest footwall unit overthrust by Upper Triassic to Lower Cretaceous shallow- to deep-marine sedimentary succession in a hanging wall of the SE-dipping ČMT (Fig. 4 ). The Oštrc Fm. turbidites are characterized by meter- to meso-scale tight asymmetric folds with NE-SW trending and dominantly SW-dipping fold axes (Figs. 5 a, b). In the same formation, this folding is associated with axial plane cleavage (Fig. 5 a, b). Moreover, in the underlying Aptychus limestone, similar but predominantly open asymmetric folds are documented showing the same fold axes orientation. Overall consistency of fold asymmetries and SE-dipping axial planes and axial plane cleavage (Figs. 5 a, b) with respect to the stratification, indicate NW-ward direction of tectonic transport, which is in accordance with tectonic transport direction of the overlaying SDII and the ČMT kinematics. 3.1.2. Structural domain Ivanščica Imbricates (SDII) This structural domain occupies southern parts of central and eastern Ivanščica Mt. To the northwest, domain thrusts over the SDIP by the SE-dipping ČMT floor thrust (Figs. 2 , 3 , 4 ). In the south, it is unconformably overlain by Oligo-Neogene cover (Figs. 2 , 3 and 4 ). The main structural characteristic of this domain is a series of SE-dipping reverse faults splay off from the ČMT floor thrust (decollement), thus forming a stack of NW-verging imbricates in the present-day orientation (Figs. 2 , 4 ). These imbricates are made of Upper Triassic platform carbonates overlain by Lower Jurassic to Lower Cretaceous pelagic succession, which dips underneath the ophiolitic mélange of Repno Complex previously tectonically emplaced over this pelagic succession (Figs. 2 , 4 ). Thus, the formation of these imbricates postdates the emplacement of the ophiolitic mélange. The lithostratigraphic composition of imbricates changes in NW direction in a way that Repno complex thrusts over progressively younger formations starting with Lower Jurassic up to lowermost Cretaceous pelagic deposits (Figs. 2 , 4 ). The Oštrc Fm. is present only in the NW-most imbricate, locally stuck between the ČMT and the antithetic reverse fault here named the Babin Zub back-thrust (BZBT; Figs. 2 , 4 ). Formation of the BZBT was probably favoured by a steep ramp in the SE-dipping ČMT (Fig. 4 ). SE vergence of the BZBT is supported by geometry of the overturned syncline with its parasitic folds and axial plane cleavage well developed in the pelagic Aptychus limestone and the Oštrc Fm. (Figs. 4 , 5 d-f). Thus, the BZBT and the first imbricate to the SE form a NE-striking triangle structure (Figs. 2 , 4 and 5 h). Within the SDII, with the exception of the Repno complex, bedding planes and axial plane cleavage prevailingly dip towards SE (Figs. 4 , 5 c, g). In the overturned and tight syncline formed in the hanging wall of the BZBT bedding planes and axial plane cleavage dip to the NW (Figs. 4 , 5 c-e). Outcrops of the Repno complex are characterized by pervasive scaly cleavage. Planar fabric is mainly represented by clay minerals enveloping variously sized blocks of basalt, gabbro, chert, and sandstone (Fig. 6 b). Basalt and gabbro blocks are usually tens and up to hundred meters in diameter, while chert and sandstone blocks are centimetre up to tens of meters in diameter. Well-developed kinematic indicators (S-C fabrics, asymmetric and symmetric boudins) record inconsistent sense of shear (Fig. 6 a-c). However, close to imbricates bounding reverse faults, kinematic indicators in the Repno complex show sense of shear compatible with kinematics of these faults (Fig. 6 c). In the southwestern part of the SDII, structurally the highest pre-Oligo–Neogene tectonic unit, called the Oštrc klippe thrusts over the Oštrc Fm. of the leading imbricate (Figs. 2 , 4 ). Klippe comprises Upper Triassic platform carbonates and subordinately Jurassic pelagic deposits, both folded in a form of NE-SW trending anticline (Figs. 2 , 4 ). 3.1.3. Structural domain Oligo-Neogene sedimentary cover (SDONC) Oligo-Neogene sediments of this structural domain unconformably overlay Permo-Mesozoic units and seal all structures observed in the previous two domains described above. Thus, these sediments represent post-tectonic cover with respect to structures of these two domains. This can be observed on the southern slopes of Ivanščica Mt. where none of NW-verging reverse faults in the SDII extend into Oligo-Miocene sedimentary cover (Figs. 2 , 4 ). Here, Oligo-Miocene sediments uniformly gently dip towards S-SE and except for that do not show other deformational structures. In contrast, severe tectonic deformations are observed along the northern margin of Ivanščica Mt. where sediments of this domain are overthrusted by Permo-Mesozoic units of the SDIP. In addition to this, formations of both domains the SDIP and the SDONC are severely affected by transpressional faulting along a set of generally ENE striking dextral faults (Figs. 2 , 4 , 6 d, e). This fault set separates the Lepoglava syncline from the northern part of Ivanščica Mt. and is considered as an eastward prolongation of the Šoštanj fault (Fig. 1 c; Vrabec & Fodor, 2006; Atanackov et al., 2021 ). The youngest sediments clearly affected by this dextral fault set are of Late Pannonian age, but younger cannot be excluded. Another prominent structure is SE striking Gotalovec – Prigorec dextral fault affecting uppermost Pannonian deposits (Fig. 2 ) or possibly even younger. South of Ivanščica Mt., similar dextral faults are not present or do only insignificant impact on the structural setting. Here folds and minor reverse faults of E-W to NE-SW orientation are most prominent structures (Figs. 2 , 6 ). 3.1.4. Oligocene-Quaternary structures in wider study area revealed by reflection seismic data 2D reflection seismic sections and well data are used to interpret and map structures in the subsurface in order to better understand about tectonic history of the study area. Traces of used seismic sections and positions of wells are shown in Fig. 1 c. Pervasive polyphase deformation is registered across the whole study area, encompassing the entire Oligocene-Quaternary sedimentary sequence in which five characteristic types of structures were identified: extensional listric faults, inverted extensional listric faults, folds associated with reverse faults, positive flower structures, and reverse faults (Fig. 7 ). The Oligocene-Quaternary sedimentary sequence of the research area is divided into two separate paleo-environmental evolution zones. Specifically, the oldest deposits of Oligocene age are mainly present in the area to the north of Ivanščica Mt., with a thickness of more than several hundred meters (Fig. 8 ), and they pinch-out to the south of Ivanščica Mt., where the oldest deposits are of Neogene age. The syn-rift structures are the oldest Neogene structures observed in the research area. According to reflectors geometry and seismic facies characteristics, it is possible to differentiate Early to Middle Miocene syn-rift units from older basement units (Fig. 8 ). Inside the basement, slightly inclined to horizontal echelon zones of sub-parallel, discontinuous, high amplitude reflectors are present (Figs. 7 , 8 ), interpreted as listric normal faults that merge in depth into detachment dipping towards the NE. Different generations of half-grabens developed in their hanging walls are observed on seismic sections. Based on well data, half-graben formation is constrained by thick syn-rift Lower to Middle Miocene deposits (Figs. 7 , 8 ) penetrated by the Hz-1 well (Fig. 8 ). The post-rift deposits are of late Middle Miocene and/or early Late Miocene age (Figs. 7 , 8 ). Notably, the absence of cross-cut features indicates a coherent deformation history during Early and Middle Miocene, however, in some cases with reactivation of earlier formed normal faults, and inversion of extensional listric faults into reverse faults (Fig. 7 ). This tectonic inversion is coeval with early Late Miocene deposition. Three groups of structures are observed in the deformed post-rift Upper Miocene and Pliocene deposits. The first are reverse faults with SE and NW vergence, predominantly in the area between Ivanščica and Medvednica Mt. (Figs. 7 , 8 ). Displacement on these faults is commonly several dozen up to hundreds of meters. As a result, the basement units are brought above Upper Miocene deposits in their footwalls. Between the Ivanščica Mt. and the Hz-1 well (Figs. 2 , 8 ), a general vergence of these faults is towards SE, while in between this well and Medvednica Mt. reverse faults mostly dip towards SE and have NW vergence (Fig. 8 ). These reverse faults are usually formed as by conjugate faults, and commonly bound the E-W to NE-SW striking, open and symmetric anticlines or pop-ups in their hanging walls. The most prominent structure between Ivanščica and Medvednica mountains is the Konjščina syncline (Fig. 8 ). In the core of this syncline 2000 m of Upper Miocene, Pliocene, and Quaternary deposits were penetrated by the Hz-1 well (Fig. 8 ). Onlap and downlap reflection terminations are common, but mainly connected to the syn-depositional clinoform architecture related to the basin-scale morphological shelf progradation (Fig. 8 ). However, the onlap features observed above the Upper Miocene clinoform unit around Hz-1 well, are folded together with the prominent reflector on which they onlap (Fig. 8 ). Considering the data from the Hz-1 well, this unit is represented by an alternation of sandstone and marls, which are discordantly overlain by gravels at depth of 580 m (Fig. 8 ), that is coeval with the base of the Plio-Quaternary deposits. This folded discordance surface is folded and pinching out towards Strugača anticline to the N and eastern Medvednica Mt. to the S. As observed on seismic and surface structural data, the overlying Plio-Quaternary deposits are also folded and faulted (Fig. 8 ). The next prominent syncline is the SE trending Lepoglava syncline located to the N of Ivanščica Mt. between two regional dextral faults, the Šoštanj fault to the S and Donat fault to the N (Figs. 1 , 2 ). 3.2. Vitrinite Reflectance Vitrinite reflectance (VR, %R o ) was measured on isolated organic matter using Zeiss Axio Imager microscope equipped with MSP 210 microscope spectrometer (oil immersion) following standard procedures (Stach et al., 1982 ; Taylor et al., 1998 ). Firstly, total organic carbon content (TOC) was determined on selected samples (siltstones and mudstones of Cretaceous, Jurassic, and Triassic age). The TOC content was measured on Leco C744 carbon analyser. To remove carbonates samples were pre-treated with hot 18% HCl. Then, organic matter (kerogen) was isolated. Organic matter concentrate was obtained after standard HCl/HF/ZnCl 2 treatment of rock. Standards used for calibration were Spinel (0.426%R o ), Sapphire (0.596%R o ), Yttrium-Aluminum-Garnet (0.905%R o ), Gadolinium-Gallium-Garnet (1.721%R o ), Cubic-Zirconia (3.12%R o ), Strontium-Titanate (5.38%R o ). VR was converted to peak paleotemperatures using formulas defined by Barker & Pawlewicz ( 1994 ) for burial heating (T peak =(lnRr + 1.68)/0.0124). Organic matter was examined on Olympus BX-51 microscope. The organic matter content in analysed siltstones and mudstones ranges from 0.16 to 1.16 wt. % TOC (Table 1 ). Generally, organic matter content is low (TOC < 0,3%) except in Jurassic (GV-476) and Triassic (GT-240) siltstones (0,91 and 1,16% TOC, respectively). Organic matter is mainly fine detrital and of terrigenous origin, represented either with vitrinite macerals or with dark, non-fluorescent, highly thermally altered amorphous organic matter. Inertinite, mainly fusinite particles are evidenced as well. Table 1 Vitrinite Reflectance Analytical Data Coordinates Sample (domain) Lithology Latitude Longitude TOC Leco (%) VR %R o No. SD %R min %R max TAI Conversion TAI-%R o T peak (⁰C) Range T peaK (⁰C) GV-224 (SDIP) Lower Cretaceous Siltstone 46.174581 16.066425 0,31 2,10 35 0,27 1,63 2,57 4 − 2–3 200 180–220 GV-1416 (SDII) Lower Cretaceous Siltstone 46.163606 16.093678 0,16 4 > 3 > 230 > 230 GV-1633 (SDII) Lower Cretaceous Siltstone 46.162534 16.061793 0,22 2,19 24 0,21 1,80 2,54 4 − 2–3 200 190–220 DJI-8,30 (SDIP) Lower Cretaceous Siltstone 46.175544 16.073502 0,20 4 − 2–3 > 200 190–220 GV-476 (SDII) Jurassic Siltstone 46.159107 16.096391 0,91 1,81 140 0,18 1,44 2,27 3 + -4 − 1,8 − 2,2 185 170–200 GV-1257A (SDII) Jurassic Siltstone 46.156935 16.121706 0,27 4 − 2–3 > 200 > 200 GV-1257B (SDII) Jurassic Siltstone 46.156935 16.121706 0,21 4 − 2–3 > 200 > 200 GV-1477 (SDII) Lower Jurassic Mudstone 46.172566 16.159687 0,19 2,93 7 0,30 2,45 3,26 4 − 2–3 225 210–230 GV-1585 (SDII) Lower Jurassic Mudstone 46.174929 16.161486 0,24 1,86 5 0,07 1,76 1,95 3 + -4 − 1,8 − 2,2 190 180–190 MR-24,50 (SDII) Lower Jurassic Mudstone 46.164998 16.135985 0,26 1,95 45 0,53 0,92 2,80 3 + -4 − 1,8 − 2,2 190 135–220 GV-113 (SDIP) Middle Triassic Siltstone 46.192836 15.98391 0,40 4 > 3 > 230 > 230 GT-240 (SDIP) Middle Triassic Siltstone 46.181091 16.196046 1,16 3,84 31 0,42 3,05 4,71 4 > 3 245 220–260 The data are discussed in the text. Abbreviations: TOC = total organic carbon; VR = vitrinite reflectance; No = number of measurements; SD = standard deviation; R min = minimum vitrinite reflectance; R max = maximum vitrinite reflectance; TAI = thermal alteration index; SDII = structural domain Ivanščica imbricates; SDIP = structural domain Ivanščica parautochton; o.m. = ophiolitic mélange. Middle Triassic organic matter is highly thermally altered. VR (3,84%R o ) correspond to paleo-temperatures of ≥ 245 ⁰C (Bostick, 1979 ; Barker & Pawlewicz, 1994 ; Rainer et al., 2016 ). Organic matter in Lower Jurassic mudstones is mainly amorphous while in Jurassic siltstones vitrinite macerals prevailed. VR and TAI in all Jurassic samples indicate transition from catagenesis into metagenesis except in GV-1477 sample. VR in GV-1477 is higher (2.93%Ro) than in two others measured (1,86 and 195, respectively) pointing to higher paleotemperatures (> 225 ⁰C) in that sample in relation to other ones (≈ 190 ⁰C). According to VR and TAI Lower Cretaceous siltstones have reached onset of metagenesis. VR is slightly higher than 2%R o indicating paleotemperatures ≥ 200 ⁰C. 3.3. Apatite Fission Track Apatite fission track (AFT) analyses was carried out by Institute of Geology at Czech Academy of Sciences. Samples for AFT analysis were collected from both Permo-Mesozoic structural domains to compare their thermal histories and reconstruct the uplift path of the Alpine – Dinaridic transitional zone. Since the study area consists mostly of carbonate sedimentary rocks and thus lacking apatite-rich lithologies, we selected the only three potentially suitable lithostratigraphic units for apatite extraction. Among overall eight samples collected from Permian to Lower Triassic sandstones, Middle Triassic volcanic rocks and Lower Cretaceous turbidites, only three samples from Permian to Lower Triassic sandstones gave enough apatites for analysis and only two of them (GV-1609 and GV-1625; Fig. 2 ) were successfully analysed. The apatites extraction from the rock samples (8 kg per sample) was done following standard mineral separation (REF) and their preparation for counting and subsequent measurement of uranium content by using LA-ICP-MS (Laser Ablation Inductively Coupled Plasma Mass Spectrometry) following the procedure and age calculation described by Hasebe et al. ( 2004 ). IsoplotR software (Vermeesch, 2018 ) and Durango apatite standard were used for zeta factor calculation and final calculation of ages. The results of two AFT analyses are presented in Table 2 . Two analysed detrital samples from the SDIP yield a central age of 56.36 ± 2.50 Ma for GV-1609 and 67.27 ± 5.38 Ma for GV-1625 (Fig. 8 ). Measured mean track length is 11.12 ± 2.54 µm for the sample GV-1609 and 11.76 ± 1.76 µm for the sample GV-1625. The AFT age and length measurements were combined with paleo temperature and stratigraphic constraints in order to derive the cooling trajectories for both samples by using HeFTy software based on fission track annealing algorithms (Ketcham, 2005 ; Ketcham et al., 2007 ). The obtained time-temperature model of both samples (Fig. 8 ) indicates fast, tectonically induced cooling that took place immediately after peak temperature conditions that were reached in the Early Cretaceous (ca. 140 Ma). Model suggests a drop of a temperature from a minimum 300 ⁰C to 100 ⁰C between 140 and 125 Ma and a cooling rate of a minimum 13.33 ⁰C/Ma. This implies denudation rate of 0.53 km/Ma if assume an average thermal gradient of 25 ⁰C/km. The length of the apatite fission tracks corrected for the angle of measurement indicate subsequent relatively slow cooling period through the apatite partial annealing zone (APAZ) and following stable period with only minor fluctuations around the lower temperature limit of the APAZ (Fig. 9 ). Table 2 Apatite Fission Track Analytical Data Coordinates Sample Lithology Latitude Longitude Central age (Ma ± 1σ) N Gr ρ s (N S ) (10 5 cm − 2 ) 238 U (ppm) 2σ MSWD P(χ2) Disp. (%) Pooled age (Ma ± 1σ) MTL (µm ± SD L ) N L D par (µm) GV-1609 Upper Permian sandstone 46.20068 16.08756 56.36 ± 2.5 63 0.09 (3396) 21.50 1.03 5.5 0 28.43 ± 3.54 11.12 ± 2.54 40 1.90 GV-1625 Lower Triassic sandstone 46.20293 16.06070 67.27 ± 5.38 39 0.24 (1788) 26.90 0.99 7 0 42.29 ± 6.19 56.2 ± 8.5 11,76 ± 1.76 37 1.74 The data presented in table are discussed in the text, see also Fig. 8 . Abbreviations: N Gr = number of dated apatite crystals; ρ s = spontaneous track densities; N S = sum of spontaneous fission-tracks; 238 U = mean 238 U content value; MSWD = mean square of weighted deviates; P(χ2) = probability of obtaining chi-square (χ2) for n degrees of freedom (n is the number of crystals); Disp. = dispersion in single-grain ages; MTL = C axis projected mean track length with ± the standard deviation (SD L ); N L = number of measured confined tracks; D par = average etch pit diameter. 4. Discussion 4.1. Tectonic evolution of the study area and correlation with the Dinarides and the Alps Integration of structural, AFT and VR data, together with the existing sedimentological and biostratigraphic data, enabled reconstruction of the five deformational events that affected Permo-Mesozoic and/or Cenozoic formations of Ivanščica Mt. In addition, based on lithostratigraphic characteristics of volcano-sedimentary successions and their superposition, two older Mesozoic extensional events are also supposed. These events are discussed below in the context of the tectonic evolution of Ivanščica Mt. and in the context of tectonic evolution of the Dinarides and Southern-Eastern Alps. The chronology of deformational events was partly derived from overprinting relations between documented deformational structures and partly based on new biostratigraphic ages of Mesozoic successions (Vukovski et al., 2023 ) considered as pre-, syn- and post-tectonic deposits with respect to particular deformational events. Additional time constraints were established based on AFT data. 4.1.1. Pre-Cretaceous tectonic evolution The oldest deformational event (D1) on Ivanščica Mt., although not directly confirmed by deformational structures, is proposed here due to the presence of syn-rift volcano-sedimentary successions of Middle Triassic age. Namely, Anisian to Ladinian pelagic successions documented in the structural domain SDIP (Fig. 2 ), are interpreted as deposited in a relatively deep depocenters arranged in a form of half-grabens controlled by steep normal faults (Goričan et al., 2005 ; Slovenec et al., 2020 , 2023 ; Kukoč et al., 2023 ). On Ivanščica Mt., the oldest pelagic deposits are Illyrian radiolarian cherts (Goričan et al., 2005 ; Slovenec et al., 2020 ; Kukoč et al., 2023 ), while on nearby Kuna gora Mt. ammonites dating of pelagic limestones indicate their Pelsonian age (Kukoč et al., 2023 ). Thus, this oldest deformational event (D1) is assumed as extensional and related with the opening of the Neotethys Ocean during Middle Triassic times. These half-graben depocenters were short-lived, and a shallow-marine carbonate sedimentation was re-established again in the Late Ladinian (Šimunić & Šimunić, 1997 ; Goričan et al., 2005 ). Anisian-Ladinian extensional event is well-documented throughout the Alps and the Dinarides, characterized by deposition of coeval and lithologically similar volcano-sedimentary successions (for correlation, see Kukoč et al. 2023 ). During Early Jurassic, after a period of Late Triassic shallow-marine sedimentation proved by Upper Triassic carbonates found in both pre-Oligocene structural domains of Ivanščica Mt. (i.e., in SDIP and SDII domains), a dramatic change in depositional environments took place. In the SDIP, deposition of shallow-marine carbonates continued from Late Triassic into Early Jurassic until the Pliensbachian. In contrast, in the SDII the Upper Triassic shallow-marine carbonates are covered by Lower Jurassic pelagic deposits. This dramatic deepening of depositional environments is assumed as related to yet another extensional event of Early Jurassic age (D2). As SDIP and SDII domains are separated by the ČMT (Figs. 2 , 3 and 4 ), this NW-verging thrust (recent orientation) is likely an inverted Early Jurassic normal fault. However, since Pliensbachian, pelagic conditions prevailed in both structural domains (Vukovski et al., 2023 ). This Early Jurassic extensional event correlates well with Jurassic rifting recorded in the Dinarides (reference) and in the Southern and Eastern Alps, where similar lithostratigraphic successions are documented in (e.g. Bohm, 2003; Goričan et. al 2012 ; Rožič et al. 2017 ). There, this Early Jurassic extension led to formation of the Alpine Tethys passive continental margin (e.g., Froitzheim & Eberli, 1990 ; Froitzheim & Manatschal, 1996 ). 4.1.2. Early Cretaceous tectonic evolution Tectonic emplacement of the Repno Complex over the stratigraphic succession of the Adriatic continental passive margin recorded in the SDII (Figs. 2 , 4 ) marks the oldest contractional event recorded on Ivanščica Mt. (D3). The age constraint for this event on Ivanščica Mt. is provided by the youngest formation directly overthrusted by the Repno Complex, which is uppermost Tithonian to Valanginian Aptychus limestone (Fig. 4 ). This indicates that the D3 event occurred during the Valanginian or slightly earlier. The peak temperature conditions of approximately 200°C recorded in the passive margin successions within the SDII (Table 1 ) were likely reached during this event. The obtained temperatures, calculated using the vitrinite reflection method, are only slightly higher than those estimated from the colour of pollen and dinoflagellate cysts obtained from the Repno Complex (Babić et al. 2002 ). This is in line with the structurally higher position of the Repno Complex with respect to the underlying passive margin successions. Late Jurassic to earliest Cretaceous obduction of the Neotethyan ophiolites on the eastern continental margin of Adria is well documented throughout the Dinarides and the Hellenides (e.g., Bortolotti et al., 2013 ; Tremblay et al., 2015 ; Nirta et al., 2018 with references). It is proposed that this obduction is responsible for a low-grade metamorphic overprint recorded in Paleo-Mesozoic units of the distal Adriatic margin underlaying the ophiolites (e.g., Tomljenović et al., 2008 ; Porkolab et al. 2019 ; Mišur et al., 2023 ). On Medvednica Mt., monazite dating indicate Berriasian metamorphic event (~ 143 Ma; Mišur et al. 2023 ), while in the central Dinarides, K/Ar ages indicate Tithonian to Valanginian age of this metamorphic overprint (150–135 Ma; Porkolab et al. 2019 ). Therefore, Valanginian age assumed for the D3 deformational event on Ivanščica Mt. is only slightly younger than these metamorphic ages. However, as Permian to Lower Cretaceous formations of Ivanščica Mt. are not affected by this metamorphic overprint but only a minor thermal alteration, at the time of the obduction they were in a more external (i.e., continentward) paleogeographic position on the Adriatic margin than units affected by this metamorphism. In the central Dinarides, the youngest deposits directly overthrusted by the Neotethyan ophiolites and ophiolitic mélange have so far been described from the East Bosnian-Durmitor thrust sheet where the ophiolitic mélange is found in a tectonic position above Tithonian to Berriasian pelagic limestone (Vishnevskaya et al., 2009 ). This limestone is correlative to the Apthychus Limestone from Ivanščica, although its age is constrained within a shorter stratigraphic range. Middle Triassic to Lower Cretaceous succession exposed on Ivanščica Mt. and attributed to the Adriatic continental margin correlates well with contemporaneous successions described from the Pre-Karst zone of the central Dinarides (Vukovski et al., 2023 with references). Population of detrital zircons from the Oštrc Fm. with an Early Cretaceous cooling ages (ca. 145 − 134 Ma; Lužar-Oberiter et al., 2012 ) was sourced from these more internal units (e.g. Medvednica Mt.), where zircons were reset due to obduction (D3) and exhumed during subsequent D4 event. The following contractional event recorded by deformational structures documented in the SDII and SDIP of Ivanščica Mt. is here assigned as D4 event. It resulted in formation of contractional structures observed at different scales of observation. These include NW-vergent imbricates of the SDII, which comprise Upper Triassic and Jurassic Adriatic passive margin succession together with the overlying Repno Complex (Figs. 4 , 10 ). NW-ward directed thrusting of the SDII over the SDIP along the ČMT (Fig. 4 ), the formation of the BZBT (Figs. 4 , 5 h), NW-ward reverse faulting in the SDIP (Fig. 2 ) and intense pervasive folding of non-competent Jurassic to Early Cretaceous pelagic deposits within both structural domains are also attributed to this deformational event (Figs. 5 a-f). Sedimentological evidence supports a late Early Cretaceous age of this contractional event. The youngest deposits affected by this event are turbidites of Hauterivian to Albian Oštrc Fm., thus indicating that this event should be at least partly post Albian in age. However, as the Oštrc Fm. contains lithoclasts of the underlying latest Tithonian to Valanginian Aptychus limestone (Zupanič et al., 1981 ), we consider this formation as syntectonic with respect to D4 deformational event. In addition to lithoclasts of the Aptychus limestone, the Oštrc Fm. contains other shallow-marine to pelagic lithoclasts of Triassic-Jurassic age, as well as mafic volcanic lithoclasts and abundant Cr-spinel grains (Zupanič et al., 1981 ). The source of all these lithoclasts and Cr-spinels is seen in the imbricates of the SDII. This indicates a strong, tectonically induced, fast synsedimentary Hauterivian to Albian exhumation and erosion of the uppermost Triassic to lowermost Cretaceous Adria passive margin succession together with tectonically overlaying Repno complex. This is in accordance with our AFT time-temperature models (Fig. 9 ) suggesting fast tectonically induced Early Cretaceous cooling and exhumation. The upper age limit of D4 event cannot be precisely constrained on Ivanščica Mt. due to the lack of post-tectonic cover deposits older than Oligocene. However, on the neighbouring Medvednica Mt. correlative deformational event, D1 of van Gelder et al. ( 2015 ) or D2 of Tomljenović et al. ( 2008 ), predates the Late Cretaceous transgression and deposition of the Gosau-type sediments (Glog Fm.; Lužar-Oberiter et al., 2012 with references). Considering an Oligocene-earliest Miocene c. 130° rotation of the block carrying Medvednica and neighbouring northern Croatian mountains (including Ivanščica) proposed by Tomljenović et al. ( 2008 ), the original trend of the D4 deformational structures documented on Ivanščica would be NW-SE and with SW-ward direction of tectonic transport. In that case, the initial pre-Miocene orientation and vergence of the D4 structures on Ivanščica Mt. would correspond well with contemporaneous and commonly observed SW verging structures in the Internal Dinarides (e.g., Schmid et al., 2008 ; Schefer, 2010 ; Porkolab et al., 2019 , Nirta et al., 2020 ). The thermal alterations recorded in Mesozoic sediments of the SDIP likely reflect D4 deformational event, since unlike the SDII, the SDIP was not overthrusted by an ophiolite nappe. Instead, continuous sedimentation of the Oštrc Fm. on top of the Aptychus limestone is recorded in the SDIP (Figs. 2 , 4 ). Therefore, we propose that peak temperature conditions in the SDIP were reached during D4 thrusting of the SDII over the SDIP, soon followed by the exhumation and cooling due to propagation of this thrusting towards the Adriatic foreland. In-sequence D4 thrusting is supported by the presence of the syn-tectonic Oštrc Fm. exclusively found in the leading sector of the SDII imbricate fan (Figs. 2 , 4 and 10 ). In the central Internal Dinarides, contractional deformational event correlative with the D4 documented on Ivanščica postdates the ophiolite obduction and predates the deposition of Upper Cretaceous ‘overstepping’ sequences (see in Nirta et al., 2020 ). Here, this event is manifested in SW-ward nappe stacking, exhumation, erosion and redeposition of passive margin units of the distal Adriatic margin together with overlaying ophiolitic units (Schmid et al., 2008 ; Schefer 2010 ; Tremblay et al., 2015 ; Porkolab et al., 2019 ; Nirta et al., 2020 ), also affecting the syn-orogenic turbiditic Vranduk Fm. and its proximal equivalent the Pogari Fm. (Mikes et al., 2008 ; Nirta et al., 2020 ). These formations are corelative with syn-orogenic Hauterivian to Albian Oštrc Fm. and Aptian–Albian shallow-water Bistra Fm. (Gušić, 1975 ; Crnjaković, 1989 ; Lužar-Oberiter et al., 2012 ) unconformably overlying the Repno Complex in Medvednica Mt. Still, Oštrc and Bistra formations are younger than the Vranduk and Pogari formations (Mikes et al., 2008 ; Nirta et al., 2020 with references therein; Hrvatović, 2022 ), thus suggesting younger age of D4 deformations and more forelandward position of Ivanščica Mt. during this event. In the Eastern Alps, Early Cretaceous contractional deformational event correlative with D4 event of Ivanščica is well-known as Eo-Alpine event characterized by WNW-ward stacking of the Austroalpine nappe units (Neubauer et al., 1999 ; Schmid et al., 2008 , 2020 and references therein) and a deposition of the syn-orogenic Rossfeld Formation of a Late Valanginian to Aptian age (~ 135 − 110 Ma; Faupl & Wagreich, 2000 ). Moreover, regional Early Cretaceous event is documented along whole East Alpine-Dinaridic-Hellenic belt (Neubauer et al., 1999 ; Schefer, 2010 ; Bortolotti et al., 2013 ), including Wester Carpathians (Plašienka et al., 1997a , b ). In general, it is interpreted as related to the closure of the northern branch of the Neotethys Ocean (Schmid et al., 2008 ; 2020 ; Nirta et al., 2018 , 2020 ). The D4 event resulted with a regional emersion recorded on Ivanščica Mt. as well as throughout the Dinarides and the Eastern Alps. The oldest sediments covering Mesozoic formations on Ivanščica Mt. are lowermost Miocene clastic deposits found on the southern slopes (Fig. 2 ). Locally across the Dinarides, this emersion was considerably shorter and lasted until the Late Cretaceous when ‘overstepping sediments’ were deposited on top of Mesozoic formations (Nirta et al., 2020 ; Hrvatović, 2022 ). Similarly, in the Medvednica Mt. these sediments are known as Gosau-type deposits and are of Santonian to Paleocene age (Crnjaković, 1979 ). Additionally, lateritic sediments on top of serpentinites are found at the base of Campanian rudist limestone (Palinkaš et al., 2006 ; Moro et al., 2010 ). Another evidence of emersion can be found in bauxite deposits on the neighbouring Ravna gora Mt. formed on top of Triassic dolomites, likely exhumed during the D4 event. Bauxites are sealed by Middle and Upper Eocene foraminiferal limestone (Šimunić et al., 1981 ; Šimunić, 1992 ). Post Early Cretaceous emersion in the study area suggests that Late Cretaceous to Eocene sedimentary burial cannot be the explanation for the thermal alteration, as it is interpreted for the area of Sava folds and further westward in Slovenian Basin where continuous latest Cretaceous to Middle Eocene sedimentation resulted in deposition of at least 5 km of flysch type sediments (Rainer et al., 2016 ). Records of this emersion, which lasted from latest Jurassic – earliest Cretaceous until the Late Turonian transgression and the deposition of the Lower Gosau Group are found in the Austroalpine unit and the Western Carpathians (Wagreich & Faupl, 1994 ; Wagreich & Marschalko, 1995 ; Stern & Wagreich; 2013 ; Steiner et al., 2021 ). The cooling trajectories of AFT samples obtained in this study indicate a tectonically stable period with only minor fluctuations after the fast cooling related to the D4 event (Fig. 9 ). Obtained central ages of 56.4 ± 2.5 Ma for sample GV-1609 and 67.3 ± 5.4 Ma for sample GV-1625 are result of a long-lasting stay of these samples around the lower limit of the APAZ (Fig. 9 ). For that reason, we suppose that the SDIP and the SDII were not affected by any major deformation postdating D4 Early Cretaceous contraction and predating D5 Early Miocene extension. 4.1.3. Neogene-recent tectonic evolution NE dipping low angle listric normal growth faults documented on reflection seismic sections (Fig. 7 ), associated with ENE striking dextral strike-slip faults around the prominent Early Miocene syn-rift depocenters N of Ivanščica Mt. (Figs. 1 c, 2 ) are attributed to the D5 deformational event that resulted with Early Miocene NE-SW directed extension. The D5 normal faults crosscut older structures (Fig. 4 ) with only sporadic evidence for their later inversion or reactivation. Termination of D5 extension is marked by the Late Badenian transgression and deposition of clastic to carbonate sediments, which seal Early Miocene rift structures (Figs. 7 , 8 ). The termination of this event corresponds with a gradual decrease in volcanic activity during late Middle Miocene in the Pannonian basin (Balázs et al., 2016 ; Pavelić & Kovačić, 2018 ). Onlapping of Pannonian over Sarmatian sediments indicate a Late Sarmatian short-lived contraction (D6), also documented in reflection seismic sections near Medvednica Mt. by Tomljenović & Csontos ( 2001 ). It resulted in partly reactivation of the D5 normal listric faults into reverse faults (Fig. 7 ). The subsequent stage of thermal subsidence well documented across the entire Pannonian basin area was characterised by filling of accommodation space and gradual filling of the basin during Late Miocene and Pliocene times (Kovačić et al., 2004 ; Sebe et al., 2020 ). The youngest deformation event (D7) is constrained to Late Miocene to present, characterized by NNW-SSE contraction. To the north of Ivanščica Mt., this contraction is accommodated by the reactivation of ENE striking dextral faults (e.g. Šoštanj fault; Fig. 6 d, e) and by formation of E to NE trending km large folds and SE striking dextral faults (Fig. 2 ). Here, reverse faulting is mostly accommodated along local transpressional ramps of major strike-slip faults. The influence of strike-slip faulting diminishes sharply to the south at the N to NW vergent Northern Ivanščica reverse fault (Figs. 2 , 4 ), which possibly represents Early Cretaceous D4 fault reactivated during D7 Late Miocene-present contraction. This fault is responsible for NW-ward high angle thrusting of the Permo–Mesozoic units of the SDIP and passively transported SDII over Upper Oligocene to Lower Miocene deposits, inclination of homoclinal S to SE dipping Miocene strata in the southern slopes of the mountain (Fig. 4 ), and final uplift of Ivanščica. SE striking Gotalovec – Prigorec dextral fault is attributed to D7 event according to Late Pannonian age of deformed strata. To the south towards Medvednica Mt., same NNW-SSE contraction resulted in formation of series of E to NE trending, tens kilometres long anticlines and synclines, with small offset reverse faults developed in the limbs of anticlines (Figs. 7 , 8 ). Onlapping and thinning of syn-tectonic strata along the flanks of anticlines indicate that the main stage of folding started in the late Pannonian (Figs. 7 , 8 ). This deformation and timing corelates well with previous field kinematic studies and interpretations of seismic data from wider study area (Placer, 1999b ; Tomljenović & Csontos, 2001 ; van Gelder et al., 2015 ; Balázs et al., 2016 ). 4.2. Tectonic position of Ivanščica Mt. Earlier studies considered Ivanščica, for the most part, as a S-vergent Neogene nappe of the South Alpine unit, thrusted over the ophiolitic mélange of the Western Vardar ophiolitic unit of the Dinarides (Repno complex; Fig. 1 c; Placer, 1999a ; Schmid et al., 2008 , 2020 ; van Gelder et al., 2015 ). Our investigation did not reveal any S to SE vergent thrust of the Miocene age. The only SE vergent fault is the BZBT, whose location and kinematics coincides with the frontal thrust of the South Alpine unit according to Placer, ( 1999a ), van Gelder et al. ( 2015 ) and Schmid et al. ( 2020 ). However, BZBT is sealed by Upper Oligocene and Miocene deposits (Fig. 2 ) and thus predates Oligocene–earliest Miocene rotation. Furthermore, we interpret the BZBT to be Early Cretaceous in age. Therefore, the initial top-NE vergence of the BZBT and its Early Cretaceous age oppose the interpretation about SE-ward Miocene thrust. In addition, the main shortening phase in the South Alpine unit (the Valsugana phase, ca. 14 − 8 Ma, Castelarin et al., 1992; Doglioni, 1992 ; Castellarin & Canteli, 2000 ; Zattin et al., 2003 , 2006 ), was coeval with the regional transgression and the deposition of shallow-water to pelagic sediments in the study area, including whole Pannonian Basin (Pavelić & Kovačić, 2018 and references therein). However, the same driving process which caused thrusting within the South Alpine unit, the indentation and CCW rotation of Adria, is responsible for the Late Pannonian (~ 6 Ma) to recent contraction (D7). In the area of the Dinarides and the Pannonian Basin, this contraction resulted in folding, reverse and strike-slip faulting (Tomljenović & Csontos, 2001 ; Balázs et al., 2016 ; van Unen et al., 2019a , b ). Contrary, at the same time the South Alpine unit was characterised by thrusting (Castelarin et al., 1992; Picotti et al., 2022 ). Hence, in contrast to the previous studies, our data suggests that the study area was not affected by the Miocene S-ward retro wedge thrusting of the South Alpine unit. Considering Mesozoic and Cenozoic tectono-sedimentary evolution of Ivanščica Mt. as described earlier in the discussion, we interpret Ivanščica belongs to the Pre-Karst zone of the Dinarides. 5. Conclusions Ivanščica Mt., an inselberg in the Alpine – Dinaridic transitional zone of northern Croatia, is divided into three structural domains: Ivanščica Parautochton, Ivanščica Imbricates and Oligo-Neogene sedimentary cover. By implementation of a multi-scale structural analysis, AFT, and VR data, four contractional and one extensional event have been recorded on Ivanščica Mt. In addition, two older extensional events were recognized based on the Mesozoic tectono-sedimentary record. Middle Triassic (D1) and Early Jurassic (D2) extensional events related to the opening of the Neotethys Ocean and Alpine Tethys respectively are recorded in sedimentary successions of the SDIP and the SDII. Late Berriasian to Valanginian (~ 140 Ma) contraction (D3) is manifested with tectonic emplacement of the ophiolitic mélange of the Repno Complex over the stratigraphic successions of the Adriatic passive margin in the SDII and their thermal alteration. Following contractional event (D4) manifested in NW-ward imbrication, thrusting of the SDII over the SDIP along the ČMT and thermal alteration of sedimentary succession of the SDIP. Syn-deformational Hauterivian to Albian Oštrc Fm. and our AFT modelling results provide age constraints for this deformational event (~ 133–100 Ma). When considering the post Oligo-Miocene rotations, initial NW trending and SW verging structures attributed to D4 deformational event coincide with the typical Dinaridic structural trend. This deformational event is a result of continued contraction related to the closure of the northern branch of the Neotethys Ocean and finally resulted in long lasting emersion in the Ivanščica Mt. The youngest extensional event (D5) is characterized by formation of NE-dipping predominantly listric normal faults and ENE striking dextral faults, as a consequence of ongoing extension in the Pannonian Basin. Timing of deformation is constrained by the Ottnangian to middle Badenian age (~ 18–14 Ma) of syn-rift deposits observed on the reflection seismic and well data. In the early post-rift stage, short lasting late Sarmatian contraction (~ 12 Ma) is registered (D6), preceding the main stage of the basin inversion. The youngest recorded deformational event (D7) characterised by Late Pannonian (~ 6 Ma) to recent NNW-SSE contraction, resulted in reactivation of ENE striking dextral faults, formation of new SE striking dextral faults as well as the formation of E to NE trending folds and reverse faults. This event is a result of N-ward indentation and CCW rotation of Adriatic microplate. Overall Miocene and post-Miocene deformational history of the study area is in align with well-known Pannonian back-arc tectonics starting in the Early Miocene. Our results infer that the study area was affected by tectonic processes related to the different stages of the evolution of the Neotethys Ocean, opening of the Alpine Tethys Ocean, as well as the opening and inversion of the Pannonian Basin. Complete Mesozoic and Cenozoic tectono-sedimentary evolution of Ivanščica Mt. exhibits Dinaridic affiliation and allows its placement in the Pre-Karst zone of the Dinarides. Abbreviations AFT apatite fission track APAZ apatite partial annealing zone BZBT Babin Zub back-thrust CCW counter clockwise ČMT Črne Mlake thrust Dn deformational event (n is the number indicating the relative age of the event where the number 1 is the oldest event) DLS Dinarides Lake System GPF Gotalovec-Prigorec fault MSWD mean square of weighted deviates n number of used data P(χ2) probability of obtaining chi-square (χ2) for n degrees of freedom (n is the number of crystals SDII structural domain Ivanščica imbricates SDIP structural domain Ivanščica parautochton SDONC structural domain Oligo-Neogene sedimentary cover SSZ supra subduction zone VR vitrinite reflectance Declarations Acknowledgements The authors would like to thank to Matija Šimunić for providing the photo in Fig. 5h. This research was supported by the Croatian Science Foundation under the project “Revealing the Middle Triassic Paleotethyan Geodynamics Recorded in the Volcano-Sedimentary Successions of NW Croatia” (IP-2019–04-3824). Author contribution Matija Vukovski :conceptualization, methodology, field work, analysis (structural), investigation, writing (original draft, review and editing); Marko Špelić : analysis (seismic sections), writing (original draft, review and editing); Duje Kukoč : field work, writing (original draft, review and editing); Tamara Troskot-Čorbić : analysis (vitrinite reflectance), writing (original draft, review and editing); Tonći Grgasović : field work, writing (review and editing); Damir Slovenec : writing (review and editing); Bruno Tomljenović : conceptualization, methodology, field work, writing (original draft, review and editing) Funding This research was funded by the Croatian Science Foundation under the project “Revealing the Middle Triassic Paleotethyan Geodynamics Recorded in the Volcano-Sedimentary Successions of NW Croatia” (IP-2019–04-3824). Data availability All data generated or analysed during this study are included in this article. 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Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-3991799","acceptedTermsAndConditions":true,"allowDirectSubmit":false,"archivedVersions":[],"articleType":"Research Article","associatedPublications":[],"authors":[{"id":275216988,"identity":"6311c6d3-4872-4765-b429-734189eba54a","order_by":0,"name":"Matija Vukovski","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAA40lEQVRIiWNgGAWjYHACZhBhwMbew8CQABbgIVYLzxlStTBI5MAECGjRnZFjbPCxrc6YT/Lt4RcPGOzs5jfwHvuAT4vZjRzjxJlth83YpPPSLBIYkpM3HOBLnoFXy5kzxod5zhywYZPOMTNI/Hcg2YCBxxivw6Ba6mzYJM+YGSQwHEiWbyCk5XiPcTJPBbMZmwSP8QOgFjuGAwS1tBUbzqg4bMzGk2MGDOTkBIPDhLQcZt4s8cGgznB++xnjjz8Y7Ozl23vwa0EGbBJAIrGBmWgNwDgFRYc9CRpGwSgYBaNghAAAGFNBDlxGpdMAAAAASUVORK5CYII=","orcid":"","institution":"Croatian Geological Survey","correspondingAuthor":true,"prefix":"","firstName":"Matija","middleName":"","lastName":"Vukovski","suffix":""},{"id":275216989,"identity":"f7f6a956-c2f8-4d88-8632-3389cfb159bd","order_by":1,"name":"Marko Špelić","email":"","orcid":"","institution":"Croatian Geological Survey","correspondingAuthor":false,"prefix":"","firstName":"Marko","middleName":"","lastName":"Špelić","suffix":""},{"id":275216990,"identity":"f0efe4b1-64b4-4654-80ac-f492b56b38e8","order_by":2,"name":"Duje Kukoč","email":"","orcid":"","institution":"Croatian Geological Survey","correspondingAuthor":false,"prefix":"","firstName":"Duje","middleName":"","lastName":"Kukoč","suffix":""},{"id":275216991,"identity":"ad316681-9f09-4651-8007-a695b250fc9a","order_by":3,"name":"Tamara Troskot-Čorbić","email":"","orcid":"","institution":"INA -Oil Company, Plc., Exploration \u0026 Production","correspondingAuthor":false,"prefix":"","firstName":"Tamara","middleName":"","lastName":"Troskot-Čorbić","suffix":""},{"id":275216992,"identity":"986a9c76-6764-45ff-9622-1af1b0722cd7","order_by":4,"name":"Tonći Grgasović","email":"","orcid":"","institution":"Croatian Geological Survey","correspondingAuthor":false,"prefix":"","firstName":"Tonći","middleName":"","lastName":"Grgasović","suffix":""},{"id":275216993,"identity":"9fb08263-76ce-4a8d-b73a-394ec41edc0e","order_by":5,"name":"Damir Slovenec","email":"","orcid":"","institution":"Croatian Geological Survey","correspondingAuthor":false,"prefix":"","firstName":"Damir","middleName":"","lastName":"Slovenec","suffix":""},{"id":275216994,"identity":"c5b4f6ce-6515-4b2f-9028-f7baeb0e9c31","order_by":6,"name":"Bruno Tomljenović","email":"","orcid":"","institution":"University of Zagreb","correspondingAuthor":false,"prefix":"","firstName":"Bruno","middleName":"","lastName":"Tomljenović","suffix":""}],"badges":[],"createdAt":"2024-02-26 19:33:38","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-3991799/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-3991799/v1","draftVersion":[],"editorialEvents":[{"content":"https://doi.org/10.1186/s00015-024-00464-5","type":"published","date":"2024-09-02T15:56:58+00:00"}],"editorialNote":"","failedWorkflow":false,"files":[{"id":51788033,"identity":"318943c7-00b2-4d77-b987-b8b745c16432","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":498657,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003ea\u003c/strong\u003e Topographic map of the northern Adriatic realm. Note the red polygon representing outlines of Ivanščica Mt. \u003cstrong\u003eb\u003c/strong\u003e Tectonic map after Schmid et al. (2020) showing constituent tectonic units of the Dinarides and the Alps. Ivanščica Mt. (marked with yellow line) occupies position at the junction of the Western Vardar ophiolitic unit of the Dinarides and Southern Alpine unit of the Alps in the southwestern part of the Pannonian Basin (white outlines). PFS – Periadriatic Fault System. Location of figure is shown in Fig. 1a. \u003cstrong\u003ec \u003c/strong\u003eGeological map of the Ivanščica Mt. and wider surrounding area in the Dinarides – Alps – Pannonian Basin transitional zone (simplified and modified after Basic Geological Maps of former Yugoslavia on the 1:100,000 scale, sheets Celje (Buser, 1977), Rogatec (Aničić \u0026amp; Juriša, 1984), Varaždin (Šimunić et al., 1982), Novo Mesto (Pleničar et al., 1975), Zagreb (Šikić et al., 1977) and Ivanić (Basch, 1981)). Location of figure is shown in Fig. 1b\u003c/p\u003e","description":"","filename":"VukovskietalFig1.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/d95853fd45c977644c186d45.png"},{"id":51788183,"identity":"5506f5f4-7777-483a-be19-b7d598a58edf","added_by":"auto","created_at":"2024-02-29 04:40:12","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":144512,"visible":true,"origin":"","legend":"\u003cp\u003eGeological map of Ivanščica Mt. compiled from Šimunić et al. (1982) and the results of this study. The map shows the locations of cross-sections A-A’; B-B’ and C-C’ (shown in Fig. 3) and sample locations used for apatite fission track dating. The location of the figure is shown in Fig. 1c. Abbreviations: ČMT = Črne Mlake thrust; BZBT = Babin Zub back-thrust; GPF = Gotalovec-Prigorec fault\u003c/p\u003e","description":"","filename":"VukovskietalFig2.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/9d57b625b38b8df59a28cf89.png"},{"id":51788032,"identity":"2d668632-55ee-434c-967f-78eed38846e1","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":46152,"visible":true,"origin":"","legend":"\u003cp\u003eSimplified tectonic map of the Ivanščica Mt. showing three structural domains.\u003c/p\u003e","description":"","filename":"VukovskietalFig3.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/5f4f4e35e8bf9bb35e19b10c.png"},{"id":51788035,"identity":"5418b635-7a81-4eeb-82c6-ff55a1c1a769","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":123746,"visible":true,"origin":"","legend":"\u003cp\u003eCross-sections across Ivanščica Mt. Cross-sections A-A’ and B-B’ are perpendicular to the strike of structures in SDII and SDIP. Cross-section C-C’ is longitudinal to the same structures. Positions of cross sections are shown in Fig. 2. Legend is identical to that shown in Fig. 2\u003c/p\u003e","description":"","filename":"VukovskietalFig4.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/c0d37744d1e375ffef74bd77.png"},{"id":51788042,"identity":"451651ec-4248-49d8-8f22-445257c4b4f4","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":2518978,"visible":true,"origin":"","legend":"\u003cp\u003eExamples of kinematic data. \u003cstrong\u003ea\u003c/strong\u003e Stereoplot of the D1 fold axes, axial planes and bedding-axial plane cleavage intersection lineation, projected on top of the Kamb contour plot. Mean orientation of the fold axes is 231/20. The measurements are taken from pelagic Aptychus limestone and Oštrc Fm. exposed within the SDIP. \u003cstrong\u003eb\u003c/strong\u003eTight asymmetric folding of siltstones and calcarenites of the Lower Cretaceous Oštrc Fm. exposed within the SDIP (46.172552, 16.058040). \u003cstrong\u003ec\u003c/strong\u003e Stereoplot of the poles to the S0 bedding, best fit Π-circle (shown with red line) and Π-axis. The measurements are taken from the Upper Triassic to lowermost Cretaceous deposits exposed within the SDII. \u003cstrong\u003ed\u003c/strong\u003e Slightly overturned NE dipping S0 bedding and pervasive S1 axial plane cleavage within siltstones and calcarenites of the Oštrc Fm. exposed within the SDII. Outcrop is located on the NW overturned limb of the syncline in the hanging wall of the BZBT (46.166424, 16.111421; see the cross-section B-B’ in Fig. 4) \u003cstrong\u003ee\u003c/strong\u003e NW dipping overturned S0 bedding and pervasive S1 axial plane cleavage within pelagic Aptychus limestone exposed within SDII. Outcrop is located on the NW overturned limb of the syncline in the hanging wall of the BZBT (46.166978, 16.110589; see the cross-section B-B’ in Fig. 4). \u003cstrong\u003ef\u003c/strong\u003e Second-order S-type parasitic folding of Aptychus limestone exposed within the SDII (46.164857, 16.095013). \u003cstrong\u003eg\u003c/strong\u003e Stereoplot of the D1 fold axes and bedding-axial plane cleavage intersection lineation, projected on top of the Kamb contour plot. Mean orientation of the fold axes is 251/9. The measurements are taken from the Jurassic to lowermost Cretaceous deposits exposed within the SDII. \u003cstrong\u003eh\u003c/strong\u003e Field photo of the SE dipping imbricate, NW dipping BZBT and Triangle structure in between. See Fig. 2 for the photo location\u003c/p\u003e","description":"","filename":"VukovskietalFig5.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/17358f64739599a89929b181.png"},{"id":51788039,"identity":"714f227b-ec42-499f-b4c4-8f725568abd0","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":1828200,"visible":true,"origin":"","legend":"\u003cp\u003eExamples of kinematic data. \u003cstrong\u003ea\u003c/strong\u003e Stereoplot of the D1 cleavage-cleavage intersection lineation, projected on top of the Kamb contour plot. Mean orientation of the fold axes is 50-230. The measurements are taken from the ophiolitic mélange unit exposed within the SDII. Black poles represent intersection lineation derived from NW vergent structures and red poles from SE vergent structures. \u003cstrong\u003eb\u003c/strong\u003eOphiolitic mélange exposed within the SDII (46.156851, 16.110643) embedding deformed symmetric blocks of sandstones in a shaly matrix. \u003cstrong\u003ec\u003c/strong\u003e S-C structures in the ophiolitic mélange exposed in the footwall just below the BZBT within the SDII (46.159118, 16.096405). \u003cstrong\u003ed\u003c/strong\u003e Stereoplot and associated paleostress tensor of strike-slip faults from the SDONC. Measurements were taken along a generally ENE striking strike-slip faults to the north of Ivanščica Mt. \u003cstrong\u003ee\u003c/strong\u003e Strike-slip fault from the ENE striking dextral fault zone to the north of Ivanščica Mt. (46.219420, 16.192191), fault plane 140/82, striations 228/20, dextral displacement\u003c/p\u003e","description":"","filename":"VukovskietalFig6.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/450235da709e8d6016c4f27d.png"},{"id":51788037,"identity":"7d8421f3-ea89-4b9b-b80f-d3d73f46b1d3","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":1680815,"visible":true,"origin":"","legend":"\u003cp\u003eCharacteristic deformational structures interpreted on the seismic profiles\u003c/p\u003e","description":"","filename":"VukovskietalFig7.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/758c7f348541b7d9f0695457.png"},{"id":51788040,"identity":"98e543d8-bb4d-4d20-8da1-6376e5f81d9a","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":101582,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003ea \u003c/strong\u003eRegional composite cross-section composed of three sections. Section 1-1’ is located to the north of Ivanščica Mt. Section B-B’ represents the homonymous cross-section from the Fig. 4. The legend for this section is shown in Fig. 2. Section 2-2’ is located to the south of Ivanščica Mt. and ends at the easternmost slopes of Medvednica Mt. For exact location of the composite cross-section and its sections see Fig. 1c. b Lithostratigraphic columns of penetrated deposits from the wells Va-1 and HZ-1. For the locations of the wells see Fig. 1c\u003c/p\u003e","description":"","filename":"VukovskietalFig8.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/f8f28baa9fe0fc53adb38d4d.png"},{"id":51788184,"identity":"42b3d503-6d6a-4ed8-a91f-77013bfe20a3","added_by":"auto","created_at":"2024-02-29 04:40:12","extension":"png","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":69495,"visible":true,"origin":"","legend":"\u003cp\u003eApatite fission track data. Radial plots (plots to the left) showing the distribution of cooling ages according to the relative error and standard deviation for the apatites, accompanied by a graphs showing the distribution of the track lengths in the apatites (graphs in the middle) and a t/T graphs (graphs to the right) showing the results of HeFTy modeling based on track length and age distribution of the apatite fission tracks. Abbreviations: n = number of used data; MSWD = mean square of weighted deviates; P(χ2) = probability of obtaining chi-square (χ2) for n degrees of freedom (n is the number of crystals; APAZ = apatite partial annealing zone\u003c/p\u003e","description":"","filename":"VukovskietalFig9.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/7a330e60860fcaae34728cbc.png"},{"id":51788038,"identity":"dc5240be-6896-4d4e-9cd9-f27eda769a66","added_by":"auto","created_at":"2024-02-29 04:32:12","extension":"png","order_by":10,"title":"Figure 10","display":"","copyAsset":false,"role":"figure","size":115803,"visible":true,"origin":"","legend":"\u003cp\u003eAn overview of the most important tectonic events documented on Ivanščica Mt. (Kukoč et al., 2023, Slovenec et al., 2023; Vukovski et al., 2024 and the results of this study), in the eastern Southern Alps (Doglioni \u0026amp; Bosellini, 1987; Castellarin et al., 1992; Doglioni, 1992; Sarti et al., 1992; Bertotti et al., 1993; Channell, 1996; Schönborn, 1999; Mandl, 2000), the Eastern Alps (Kozur, 1991; Ratschbacher et al., 1991; Schmid et al., 1996; Dunkl \u0026amp; Demény, 1997; Froitzheim et al., 1997; Neubauer et al., 1999; Willingshofer et al., 1999a, b; Faupl \u0026amp; Wegreich, 2000; Mandl, 2000; Böhm, 2003; Thöni, 2006; Gawlick et al., 2009; Missoni \u0026amp; Gawlick, 2011a, b; Favaro et al., 2015; Rosenberg et al., 2015; Gawlick \u0026amp; Missoni, 2019; Fodor et al., 2021), Dinarides (Gušić \u0026amp; Babić, 1970; Lanphere et al., 1975; Dragičević \u0026amp; Velić, 2002; Lugović et al., 2006; Schmid et al., 2008; Ustaszewski et al., 2009; Smirčić et al., 2018, 2020; Porkolab et al., 2019; van Unen et al., 2019a, b; Nirta et al., 2020; Šegvić et al., 2020; Balling et al., 2023; Slovenec \u0026amp; Šegvić, 2024), Pannonian Basin (Tomljenović, 2002; Tomljenović \u0026amp; Csontos, 2001; Horváth et al., 2006; Balázs et al., 2016) and nearby Medvednica Mt. (Tomljenović et al., 2008; van Gelder et al., 2015; Mišur et al., 2023). Note how the tectonic events are linked with the geodynamic processes within the Neotethys Ocean (Channell \u0026amp; Kozur; 1997, Stampfli \u0026amp; Borel, 2002; 2004, Schmid et al., 2004). Time scale after Cohen et al. (2013). Periods of subduction are shown with red lines, obduction with green lines and collision with grey lines. Extensional events are shown with blue lines, contractional with grey lines, rotation of crustal blocks with yellow lines. Abbreviations: DLS = Dinarides Lake System; SSZ = supra subduction zone\u003c/p\u003e","description":"","filename":"VukovskietalFig10.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/e904f87199eebb7f538049ea.png"},{"id":51788187,"identity":"66ea6fef-1564-4e2b-94c4-a42e4d0c1a79","added_by":"auto","created_at":"2024-02-29 04:40:12","extension":"png","order_by":11,"title":"Figure 11","display":"","copyAsset":false,"role":"figure","size":57463,"visible":true,"origin":"","legend":"\u003cp\u003eSchematic geodynamic reconstruction of the wider study area (northwesternmost Internal Dinarides) during Early Cretaceous. Different symbology is used for the faults to represent different stages in their activity as explained in the legend. Blue coloured faults were formed during D0 event related to the obduction of ophiolites and ophiolitic mélange. D0 obduction caused metamorphism in the distal domains of the Adriatic passive margin (e.g. Medvednica Mt.), while proximal domains experienced thermal alteration. Red coloured faults were formed in subsequent D1 event and are responsible for the exhumation of Adriatic passive margin successions together with overlaying ophiolitic mélange, which enable their erosion and resedimentation within turbidites of the Oštrc Fm.\u003c/p\u003e","description":"","filename":"VukovskietalFig11.png","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/8a4a8a42bd33eede592a517c.png"},{"id":64186234,"identity":"580c8918-65ef-4354-a441-9b2380128edb","added_by":"auto","created_at":"2024-09-09 16:26:05","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":8368793,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-3991799/v1/345496e1-c568-471f-87aa-06d601a941e9.pdf"}],"financialInterests":"No competing interests reported.","formattedTitle":"Unravelling the Tectonic Evolution of the Dinarides – Alps – Pannonian Basin Transition Zone: Insights from Structural Analysis and Low-Temperature Thermochronology from Ivanščica Mt., NW Croatia","fulltext":[{"header":"1. Introduction","content":"\u003cp\u003eSynchronous mountain building of neighbouring orogens often results with their complex structural architectures and overprinting relationships. Such complex relationships can only be resolved by comprehensive studies that integrate lithostratigraphic, structural and thermochronological data obtained at local to regional scales of observations. In particular, such approach is inevitable in cases when both orogens are affected by post-orogenic extensional tectonics, a geodynamic scenario known from the past and at present in almost all peri-Mediterranean orogens (e.g., Meulenkamp et al., \u003cspan citationid=\"CR69\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Jolivet \u0026amp; Faccenna, \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2000\u003c/span\u003e; Faccenna et al., \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e2004\u003c/span\u003e, \u003cspan citationid=\"CR32\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Kissling et al., \u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e2006\u003c/span\u003e). This scenario, which commonly includes post-orogenic local- to regional-scale translations and rotations of differently sized tectonic blocks dismembered from previously formed collisional nappe stacks, is also known from the Dinarides \u0026ndash; Alps \u0026ndash; Pannonian Basin transitional zone (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e; e.g., Placer, \u003cspan citationid=\"CR84\" class=\"CitationRef\"\u003e1999a\u003c/span\u003e; Haas et al., \u003cspan citationid=\"CR47\" class=\"CitationRef\"\u003e2000\u003c/span\u003e; Tomljenović et al., \u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e). Namely, this area records complex tectonic histories in the orogenic build-up of the Southern-Eastern Alps and the Dinarides, followed by several phases of extension and contraction in the tectonic evolution of the SW margin of the Pannonian Basin (e.g., Fodor et al., \u003cspan citationid=\"CR37\" class=\"CitationRef\"\u003e1998\u003c/span\u003e; Vrabec \u0026amp; Fodor, 2006; Tomljenović \u0026amp; Csontos, \u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Fodor et al., \u003cspan citationid=\"CR36\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). Here, Mesozoic formations of both orogens preserve records of geodynamic processes that resulted with opening and closure of the northern branch of the Neotethys Ocean (e.g., Pamić et al., \u003cspan citationid=\"CR80\" class=\"CitationRef\"\u003e1998\u003c/span\u003e; Pamić, \u003cspan citationid=\"CR79\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Ustaszewski et al., \u003cspan citationid=\"CR129\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; the Balkan Neotethys \u003cem\u003esensu\u003c/em\u003e van Hinsbergen et al., \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). In addition, the Alps record another, younger collisional event related to the closure of the Alpine Tethys Ocean (e.g., Neubauer et al., \u003cspan citationid=\"CR75\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Willingshofer et al., \u003cspan citationid=\"CR142\" class=\"CitationRef\"\u003e1999a\u003c/span\u003e; Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; van Hinsbergen et al., \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Both oceanic realms contemporaneously existed during a part of Mesozoic times, separating the Adria microplate and the Eurasia (e.g., van Hinsbergen et al., \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). However, during the time of their closure, which differs for each of these oceanic realms, the Adriatic microplate was in a different tectonic position with respect to the European plate: lower plate in the Dinarides, and the upper plate in the Alps (e.g., Doglioni et al., \u003cspan citationid=\"CR29\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e, \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eDue to the complex Mesozoic and Cenozoic geodynamics at the Dinarides-Southern/Eastern Alps-Pannonian Basin transitional zone (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ea, b), a detail reconstruction of tectonic and depositional history, in its part in the northern Croatia, is still little known. Among several inselbergs in this area (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec), Medvednica Mt. is the most comprehensively studied so far, providing a large data set on different topics in Mesozoic stratigraphy (e.g., Halamić et al., 1999, \u003cspan citationid=\"CR49\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Babić et al., \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2002\u003c/span\u003e, with references therein), metamorphic and igneous petrology (e.g., Belak \u0026amp; Tibljaš, \u003cspan citationid=\"CR12\" class=\"CitationRef\"\u003e1998\u003c/span\u003e; Slovenec \u0026amp; Pamić, \u003cspan citationid=\"CR110\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Lugović et al., \u003cspan citationid=\"CR64\" class=\"CitationRef\"\u003e2007\u003c/span\u003e; Judik et al., \u003cspan citationid=\"CR54\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Belak et al., \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e2022\u003c/span\u003e; Mišur et al., \u003cspan citationid=\"CR73\" class=\"CitationRef\"\u003e2023\u003c/span\u003e;), paleomagnetism, structural architecture and tectonics (e.g., Tomljenović et al., \u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e). Results of most of these studies, in combination with data from the Basic Geological Map of Yugoslavia, sheet Rogatec (Aničić \u0026amp; Juriša, \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1984\u003c/span\u003e) and sheet Varaždin (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e), were so far used in correlation of pre-Neogene tectonic units of this transitional zone with corresponding tectonic units differentiated within much wider area (e.g., Haas et al., \u003cspan citationid=\"CR47\" class=\"CitationRef\"\u003e2000\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) and across the Alpine-Carpathian-Dinaridic-Hellenic orogenic system (e.g., Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e, \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; van Hinsbergen et al., \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Compared with the neighbouring Medvednica Mt., modern data on geology of the Ivanščica Mt. were relatively scarce (Babić et al., \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Goričan et al. \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Lužar-Oberiter et al., \u003cspan citationid=\"CR66\" class=\"CitationRef\"\u003e2009\u003c/span\u003e, \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2012\u003c/span\u003e), until a series of recently published studies released by the GOST project (\u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://projectgost.wordpress.com\u003c/span\u003e\u003cspan address=\"https://projectgost.wordpress.com\" targettype=\"URL\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e). These studies provide new data set on stratigraphy (Slovenec et al. \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e, \u003cspan citationid=\"CR60\" class=\"CitationRef\"\u003e2024\u003c/span\u003e), petrology (Slovenec \u0026amp; Šegvić, \u003cspan citationid=\"CR111\" class=\"CitationRef\"\u003e2024\u003c/span\u003e; Slovenec et al., \u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e2023\u003c/span\u003e; Šegvić et al., 2022) and lithostratigraphy of the Adriatic passive margin successions (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e) tectonically assembled into the structural architecture of this mountain.\u003c/p\u003e \u003cp\u003eAs a supplement to published studies of the GOST project, this paper aims to present new and more detailed data on spatial arrangement, kinematics and age of deformational structures in Mesozoic and Cenozoic rocks of Ivanščica Mt. and its neighbouring area. These data are obtained by a multi-scale structural analysis, including geological mapping, interpretation of reflection seismic sections, vitrinite reflectance and apatite fission track methods. After a short overview on geological and structural settings of Ivanščica Mt. based on previously published data, this paper presents new data on structural architecture and low-temperature thermochronology of the study area.\u003c/p\u003e \u003cp\u003eThese data are then used to propose a sequence of deformational events in the study area, which is correlated with deformational sequences revealed in neighbouring areas of Dinarides and Southern-Eastern Alps, all together discussed in the context of tectonic evolution of the Dinarides, Southern-Eastern Alps and the SW margin of the Pannonian Basin, starting from the Middle Triassic until present. Finally, we propose a new correlation between distinguished tectonic units of Ivanščica Mt. with those known from the Internal Dinarides.\u003c/p\u003e"},{"header":"2. Geological setting of Ivanščica Mountain","content":"\u003cdiv id=\"Sec3\" class=\"Section2\"\u003e \u003ch2\u003e2.1. Lithostratigraphic characteristics\u003c/h2\u003e \u003cp\u003eIvanščica Mt. is built of Upper Paleozoic and Mesozoic sedimentary successions originating from the passive margin of the Adria microplate and its basement, the Neotethyan ophiolitic m\u0026eacute;lange and Oligocene-Quaternary sedimentary cover of the Pannonian Basin (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e; Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Aničić \u0026amp; Juriša \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1984\u003c/span\u003e). The oldest rocks on Ivanščica Mt. are Permian brown-red conglomerates, sandstones and black shales concordantly overlain by Lower Triassic clastic deposits, including sporadic1-2 m thick dolomite layer along the contact (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Šimunić \u0026amp; Šimunić, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e1997\u003c/span\u003e). Lower Triassic sediments consist of micaceous sandstones, mica siltstones, shale and marls in the lower part and dark-grey, tabular, thin-bedded limestones in the upper part (Šimunić \u0026amp; Šimunić, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e1997\u003c/span\u003e). Paleozoic and Lower Triassic deposits have spatially limited exposure on the northern slopes of the mountain. These deposits originated from a shallow-marine environment (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe largest part of the mountain is built of several hundred meters thick Middle Triassic deposits, predominantly shallow-marine dolomites and limestones (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e). Pelagic successions consisting of Anisian to Ladinian pelagic limestone and radiolarian chert intercalated with volcanic and volcaniclastic lithologies ranging from basic to acidic are also present (Goričan et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Slovenec et al., \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e2020\u003c/span\u003e, \u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e2023\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e; Smirčić et al., \u003cspan citationid=\"CR117\" class=\"CitationRef\"\u003e2024\u003c/span\u003e). These pelagic successions are several tens of meters thick, generally tectonically disturbed and their contacts with the underlying and overlying formations are rarely exposed. Middle Triassic successions reflect a period of intense tectonic activity related to the opening of the Neotethys Ocean and the formation of a horst-and-graben depositional environments as a result of extension (Goričan et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). Deep-marine basins formed during this period were relatively short-lived and carbonate platform sedimentation was reestablished in the late Ladinian (Goričan et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e). Upper Triassic sediments of Ivanščica Mt. are exclusively shallow-marine and consist of several hundred meters thick series of dolomites and limestones (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Šimunić \u0026amp; Šimunić, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e1997\u003c/span\u003e). These are the equivalent of the Main Dolomite and Dachstein Limestone found in the Alps (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eLower Jurassic to Lower Cretaceous deposits are exposed in the central part of Ivanščica Mt. Successions composed of these deposits differ in the southern and northern parts of central Ivanščica. In the northern part, shallow-marine Lower Jurassic limestone conformably overlie Upper Triassic carbonates and are in turn overlain by Middle Jurassic pelagic limestone (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). In the southern part, Upper Triassic deposits are overlain by Lower Jurassic thick pelagic series consisting of pelagic limestone, carbonate breccia, marl and calcarenites (Babić, \u003cspan citationid=\"CR4\" class=\"CitationRef\"\u003e1974\u003c/span\u003e; Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). Middle to Late Jurassic radiolarian cherts are recorded in both areas, however, their contact with underling deposits and complete thickness is not known. In both areas, radiolarian cherts conformably pass up-section into Tithonian to Valanginian pelagic Aptychus limestone with several beds of calcarenites sporadically occurring at the contact as recorded in the southern part of central Ivanščica (Babić \u0026amp; Zupanič, \u003cspan citationid=\"CR5\" class=\"CitationRef\"\u003e1973\u003c/span\u003e; Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). The youngest Mesozoic deposits are mixed carbonate-siliciclastic turbidites of the Hauterivian to Albian Oštrc Formation (Zupanič et al., \u003cspan citationid=\"CR146\" class=\"CitationRef\"\u003e1981\u003c/span\u003e; Lužar-Oberiter et al., \u003cspan citationid=\"CR66\" class=\"CitationRef\"\u003e2009\u003c/span\u003e, \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2012\u003c/span\u003e), which overly the Aptychus limestone.\u003c/p\u003e \u003cp\u003eUpper Triassic to Lower Cretaceous sedimentary successions of Ivanščica Mt. are interpreted as deposited on the eastern passive margin of the Adria microplate, which was facing the evolving Neotethys Ocean from the Middle Triassic until the ophiolite obduction in latest Jurassic-earliest Cretaceous (Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e, \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Sedimentation on this margin reflected regional tectonic activity as well as changes in ocean fertility during this period. Resedimented shallow-marine material was likely supplied from the adjacent Adriatic Carbonate Platform (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). The turbidites of the Oštrc Fm. have been interpreted as deposited in a clastic wedge in front of the advancing nappes carrying the Neotethys ophiolites (Lužar-Oberiter et al., \u003cspan citationid=\"CR66\" class=\"CitationRef\"\u003e2009\u003c/span\u003e, \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2012\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eOn the southern slopes of Ivanščica Mt., in its central and eastern parts, an ophiolitic m\u0026eacute;lange is widely exposed, named as the Repno complex (Babić \u0026amp; Zupanič, \u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e1978\u003c/span\u003e; Babić et al., \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2002\u003c/span\u003e) (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). This ophiolitic m\u0026eacute;lange is composed of centimeter to hundred meters sized blocks of sandstone, chert, basalt and gabbro chaotically embedded within a shaly-silty matrix (Babić et al., \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Slovenec et al., \u003cspan citationid=\"CR113\" class=\"CitationRef\"\u003e2011\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR60\" class=\"CitationRef\"\u003e2024\u003c/span\u003e). It is interpreted as formed during the Middle Jurassic supra-subduction in the northern branch of Neotethys Ocean and subsequent Late Jurassic to earliest Cretaceous obduction of ophiolites of this oceanic realm on the eastern Adriatic margin (Babić et al., \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR60\" class=\"CitationRef\"\u003e2024\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe oldest Cenozoic deposits on Ivanščica Mt. comprise around 350 m thick Late Egerian clastic deposits with coal seams (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). These deposits lay unconformably over different Mesozoic formations on the southern slopes of the mountain, or locally in tectonic contact with underlying Mesozoic formations (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). On the northern slopes, Upper Oligocene to Lower Miocene predominantly clastic deposits with marls, clays and tuffs are found in tectonic contact and dip underneath the Mesozoic formations (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). This around two kilometers thick Upper Oligocene \u0026ndash; Lower Miocene succession is interpreted as deposited within the Hrvatsko Zagorje Basin, a marginal basin of the Central Paratethys Sea (Avanić et al., \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). Its southern margin is interpreted as located along the present-day southern slopes of Ivanščica Mt. (Pavelić \u0026amp; Kovačić, \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2018\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eFurther to the south, a separate Neogene basin, named the North Croatian Basin, formed since the late Early Miocene (Pavelić, \u003cspan citationid=\"CR81\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Pavelić \u0026amp; Kovačić, \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). Deposition of Ottnangian to middle Badenian alluvial to marine succession with volcaniclastics marks the syn-rift period of the basin evolution. Further deepening of the depositional environment resulted in unification of both basins and widespread sedimentation of predominantly marls and limestones during middle Badenian (Pavelić \u0026amp; Kovačić, \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). Regional Late Badenian transgression and cassation of volcanic activity mark the end of the rifting stage and the onset of post-rift thermal subsidence (Pavelić \u0026amp; Kovačić, \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). Sarmatian and Early Pannonian were characterized by the deposition of marine to brackish marls and limestones. During the Late Miocene and Pliocene, the brackish lake was continuously infilled by the turbiditic, deltaic, and finally alluvial clastic sequence (Pavelić \u0026amp; Kovačić et al., 2018). These were overlain by Quaternary clastic deposits (Šimunić et al., \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec4\" class=\"Section2\"\u003e \u003ch2\u003e2.2. Structural characteristics\u003c/h2\u003e \u003cp\u003eStructurally, Ivanščica Mt., together with the other mountains of northern Croatia, is considered as an eastern continuation of the Sava folds (Šimunić et al. 1979, \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Šimunić \u003cspan citationid=\"CR105\" class=\"CitationRef\"\u003e1992\u003c/span\u003e; Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec), a tectonic unit first described by Winkler (\u003cspan citationid=\"CR143\" class=\"CitationRef\"\u003e1923\u003c/span\u003e) and later by Placer (\u003cspan citationid=\"CR85\" class=\"CitationRef\"\u003e1999b\u003c/span\u003e). During their work on the Basic geological map of SFRY, sheet Varaždin, Šimunić et al. (1979, \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e) considered all mapped faults on Ivanščica to be of Cenozoic age, with the main contractional deformations occurring during the Miocene. These authors interpreted Ivanščica as a N-vergent nappe, which brought Paleozoic and Mesozoic formations over Oligocene and earliest Miocene sediments during Early Miocene (in Eggenburgian). The occurrences of Triassic-Jurassic carbonates in the southern part of central Ivanščica were interpreted as erosional remains of structurally higher nappe (Šimunić et al., 1979, \u003cspan citationid=\"CR107\" class=\"CitationRef\"\u003e1982\u003c/span\u003e) or as olistoliths embedded in the Repno complex (Babić \u0026amp; Zupanič, \u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e1978\u003c/span\u003e). As we will show below, we interpret those occurrences as a stack of imbricates built of passive margin successions and the Repno complex, formed during an Early Cretaceous contractional event.\u003c/p\u003e \u003cp\u003eMore recent studies consider northern Croatian mountains, including Ivanščica Mt., to be a part of the Southern Alps unit (Placer, \u003cspan citationid=\"CR84\" class=\"CitationRef\"\u003e1999a\u003c/span\u003e). According to van Gelder et al. (\u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) and Schmid et al. (\u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e, \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e), Ivanščica exposes a part of S-vergent South Alpine nappe emplaced over the Internal Dinaridic units during Miocene times. Prior to this emplacement, the tectonic block carrying northern Croatian mountains undergone Oligocene\u0026ndash;earliest Miocene 130\u0026deg; clockwise rotation, as interpreted by Tomljenović et al. (\u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2008\u003c/span\u003e) based on paleomagnetic data measured in Upper Cretaceous deposits on Medvednica Mt. Subsequent normal faulting related to Early Miocene rifting and opening of this part of the Pannonian Basin overprinted older structures (Tomljenović \u0026amp; Csontos, \u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e). Basin inversion, which initiated in Late Miocene-Pliocene, caused folding and reverse faulting resulting in the final uplift of the north Croatian mountains (Tomljenović \u0026amp; Csontos, \u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e). This inversion was coeval with approximately 35\u0026deg; counterclockwise (CCW) rotation, active in Miocene to recent times, presumed as driven by the CCW rotation and indentation of the Adriatic microplate (Tomljenović \u0026amp; Csontos, \u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; M\u0026aacute;rton et al., \u003cspan citationid=\"CR68\" class=\"CitationRef\"\u003e2002\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e"},{"header":"3. Methods and Results","content":"\u003cdiv id=\"Sec6\" class=\"Section2\"\u003e \u003ch2\u003e3.1. Description of deformational structures\u003c/h2\u003e \u003cp\u003eIvanščica is a densely forested mountain with rather scarce high-quality geological outcrops. For this reason, extensive fieldwork was carried out. At locations considered as essential for better understanding of deformational history of study area, detail geological mapping in scales 1:25 000 and 1:5 000 was conducted. Special attention was given to the collection of data on deformation structures and kinematic data. Acquired data include measurements of orientation of bedding, meso-scale folds, axial plane cleavage, S-C fabrics, intersection lineations, fault planes and their kinematics, many of these recorded for the first time. Based on measured structural data, observed differences in deformation styles and mapped tectonic and depositional contacts shown in maps (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003e) and cross-sections (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e), the study area is subdivided into three structural domains that from bottom to top are: Structural domain Ivanščica parautochton (SDIP), Structural domain Ivanščica imbricates (SDII) and Structural domain Oligo-Neogene sedimentary cover (SDONC).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cdiv id=\"Sec7\" class=\"Section3\"\u003e \u003ch2\u003e3.1.1. Structural domain Ivanščica Parautochton (SDIP)\u003c/h2\u003e \u003cp\u003eStructural domain Ivanščica Parautochton (SDIP) comprises Permo-Mesozoic formations exposed along its northern slopes (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). This domain is cut and broken apart into two structural blocks to the west and east of the SE striking Gotalovec \u0026ndash; Prigorec dextral fault (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). In both structural blocks, this structural domain is overthrust by the SDII along the SE-dipping Črne Mlake roof thrust (ČMT; Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). On its SW margin, the SDIP is unconformably overlain by Oligo\u0026ndash;Neogene sediments. However, in part of mountain SW of the Vilinska špica peak (726 m), Middle Triassic formations of the SDIP are brought over Oligocene deposits by two NNW-dipping reverse faults, with only locally preserved original depositional contact (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). Contrary, no original depositional contacts between Oligo-Neogene cover and Permo-Mesozoic formations of the SDIP are preserved in the northern slopes of Ivanščica Mt. Here, Permo-Mesozoic formations of the SDIP are thrusted northward over Oligo-Neogene sediments (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). In the central part of the mountain, the complete and tectonically nearly undisturbed Permo-Mesozoic succession is homoclinally dipping towards S to SE below the SDII and the Oligo\u0026ndash;Neogene cover (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). This homoclinal structure of the SDIP is thrusted towards NW over the rest of Permo-Mesozoic units belonging to the same structural domain (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). These footwall units are arranged in a several SE-dipping imbricates and thrusted NW-ward over uppermost Oligocene to Lower Miocene sediments (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). The youngest strata in this homocline are Lower Cretaceous turbidites of the Oštrc Fm. representing the highest footwall unit overthrust by Upper Triassic to Lower Cretaceous shallow- to deep-marine sedimentary succession in a hanging wall of the SE-dipping ČMT (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). The Oštrc Fm. turbidites are characterized by meter- to meso-scale tight asymmetric folds with NE-SW trending and dominantly SW-dipping fold axes (Figs.\u0026nbsp;\u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ea, b). In the same formation, this folding is associated with axial plane cleavage (Fig.\u0026nbsp;\u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ea, b). Moreover, in the underlying Aptychus limestone, similar but predominantly open asymmetric folds are documented showing the same fold axes orientation. Overall consistency of fold asymmetries and SE-dipping axial planes and axial plane cleavage (Figs.\u0026nbsp;\u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ea, b) with respect to the stratification, indicate NW-ward direction of tectonic transport, which is in accordance with tectonic transport direction of the overlaying SDII and the ČMT kinematics.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec8\" class=\"Section3\"\u003e \u003ch2\u003e3.1.2. Structural domain Ivanščica Imbricates (SDII)\u003c/h2\u003e \u003cp\u003eThis structural domain occupies southern parts of central and eastern Ivanščica Mt. To the northwest, domain thrusts over the SDIP by the SE-dipping ČMT floor thrust (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). In the south, it is unconformably overlain by Oligo-Neogene cover (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003e and \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). The main structural characteristic of this domain is a series of SE-dipping reverse faults splay off from the ČMT floor thrust (decollement), thus forming a stack of NW-verging imbricates in the present-day orientation (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). These imbricates are made of Upper Triassic platform carbonates overlain by Lower Jurassic to Lower Cretaceous pelagic succession, which dips underneath the ophiolitic m\u0026eacute;lange of Repno Complex previously tectonically emplaced over this pelagic succession (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). Thus, the formation of these imbricates postdates the emplacement of the ophiolitic m\u0026eacute;lange. The lithostratigraphic composition of imbricates changes in NW direction in a way that Repno complex thrusts over progressively younger formations starting with Lower Jurassic up to lowermost Cretaceous pelagic deposits (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). The Oštrc Fm. is present only in the NW-most imbricate, locally stuck between the ČMT and the antithetic reverse fault here named the Babin Zub back-thrust (BZBT; Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). Formation of the BZBT was probably favoured by a steep ramp in the SE-dipping ČMT (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). SE vergence of the BZBT is supported by geometry of the overturned syncline with its parasitic folds and axial plane cleavage well developed in the pelagic Aptychus limestone and the Oštrc Fm. (Figs.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e, \u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ed-f). Thus, the BZBT and the first imbricate to the SE form a NE-striking triangle structure (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e and \u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003eh). Within the SDII, with the exception of the Repno complex, bedding planes and axial plane cleavage prevailingly dip towards SE (Figs.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e, \u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ec, g). In the overturned and tight syncline formed in the hanging wall of the BZBT bedding planes and axial plane cleavage dip to the NW (Figs.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e, \u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ec-e). Outcrops of the Repno complex are characterized by pervasive scaly cleavage. Planar fabric is mainly represented by clay minerals enveloping variously sized blocks of basalt, gabbro, chert, and sandstone (Fig.\u0026nbsp;\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003eb). Basalt and gabbro blocks are usually tens and up to hundred meters in diameter, while chert and sandstone blocks are centimetre up to tens of meters in diameter. Well-developed kinematic indicators (S-C fabrics, asymmetric and symmetric boudins) record inconsistent sense of shear (Fig.\u0026nbsp;\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003ea-c). However, close to imbricates bounding reverse faults, kinematic indicators in the Repno complex show sense of shear compatible with kinematics of these faults (Fig.\u0026nbsp;\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003ec). In the southwestern part of the SDII, structurally the highest pre-Oligo\u0026ndash;Neogene tectonic unit, called the Oštrc klippe thrusts over the Oštrc Fm. of the leading imbricate (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). Klippe comprises Upper Triassic platform carbonates and subordinately Jurassic pelagic deposits, both folded in a form of NE-SW trending anticline (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec9\" class=\"Section3\"\u003e \u003ch2\u003e3.1.3. Structural domain Oligo-Neogene sedimentary cover (SDONC)\u003c/h2\u003e \u003cp\u003eOligo-Neogene sediments of this structural domain unconformably overlay Permo-Mesozoic units and seal all structures observed in the previous two domains described above. Thus, these sediments represent post-tectonic cover with respect to structures of these two domains. This can be observed on the southern slopes of Ivanščica Mt. where none of NW-verging reverse faults in the SDII extend into Oligo-Miocene sedimentary cover (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). Here, Oligo-Miocene sediments uniformly gently dip towards S-SE and except for that do not show other deformational structures. In contrast, severe tectonic deformations are observed along the northern margin of Ivanščica Mt. where sediments of this domain are overthrusted by Permo-Mesozoic units of the SDIP. In addition to this, formations of both domains the SDIP and the SDONC are severely affected by transpressional faulting along a set of generally ENE striking dextral faults (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e, \u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003ed, e). This fault set separates the Lepoglava syncline from the northern part of Ivanščica Mt. and is considered as an eastward prolongation of the Šoštanj fault (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec; Vrabec \u0026amp; Fodor, 2006; Atanackov et al., \u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). The youngest sediments clearly affected by this dextral fault set are of Late Pannonian age, but younger cannot be excluded. Another prominent structure is SE striking Gotalovec \u0026ndash; Prigorec dextral fault affecting uppermost Pannonian deposits (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e) or possibly even younger. South of Ivanščica Mt., similar dextral faults are not present or do only insignificant impact on the structural setting. Here folds and minor reverse faults of E-W to NE-SW orientation are most prominent structures (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec10\" class=\"Section3\"\u003e \u003ch2\u003e3.1.4. Oligocene-Quaternary structures in wider study area revealed by reflection seismic data\u003c/h2\u003e \u003cp\u003e2D reflection seismic sections and well data are used to interpret and map structures in the subsurface in order to better understand about tectonic history of the study area. Traces of used seismic sections and positions of wells are shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec. Pervasive polyphase deformation is registered across the whole study area, encompassing the entire Oligocene-Quaternary sedimentary sequence in which five characteristic types of structures were identified: extensional listric faults, inverted extensional listric faults, folds associated with reverse faults, positive flower structures, and reverse faults (Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe Oligocene-Quaternary sedimentary sequence of the research area is divided into two separate paleo-environmental evolution zones. Specifically, the oldest deposits of Oligocene age are mainly present in the area to the north of Ivanščica Mt., with a thickness of more than several hundred meters (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e), and they pinch-out to the south of Ivanščica Mt., where the oldest deposits are of Neogene age. The syn-rift structures are the oldest Neogene structures observed in the research area. According to reflectors geometry and seismic facies characteristics, it is possible to differentiate Early to Middle Miocene syn-rift units from older basement units (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Inside the basement, slightly inclined to horizontal echelon zones of sub-parallel, discontinuous, high amplitude reflectors are present (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e), interpreted as listric normal faults that merge in depth into detachment dipping towards the NE. Different generations of half-grabens developed in their hanging walls are observed on seismic sections. Based on well data, half-graben formation is constrained by thick syn-rift Lower to Middle Miocene deposits (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e) penetrated by the Hz-1 well (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). The post-rift deposits are of late Middle Miocene and/or early Late Miocene age (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Notably, the absence of cross-cut features indicates a coherent deformation history during Early and Middle Miocene, however, in some cases with reactivation of earlier formed normal faults, and inversion of extensional listric faults into reverse faults (Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e). This tectonic inversion is coeval with early Late Miocene deposition.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThree groups of structures are observed in the deformed post-rift Upper Miocene and Pliocene deposits. The first are reverse faults with SE and NW vergence, predominantly in the area between Ivanščica and Medvednica Mt. (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Displacement on these faults is commonly several dozen up to hundreds of meters. As a result, the basement units are brought above Upper Miocene deposits in their footwalls. Between the Ivanščica Mt. and the Hz-1 well (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e), a general vergence of these faults is towards SE, while in between this well and Medvednica Mt. reverse faults mostly dip towards SE and have NW vergence (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). These reverse faults are usually formed as by conjugate faults, and commonly bound the E-W to NE-SW striking, open and symmetric anticlines or pop-ups in their hanging walls. The most prominent structure between Ivanščica and Medvednica mountains is the Konjščina syncline (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). In the core of this syncline 2000 m of Upper Miocene, Pliocene, and Quaternary deposits were penetrated by the Hz-1 well (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Onlap and downlap reflection terminations are common, but mainly connected to the syn-depositional clinoform architecture related to the basin-scale morphological shelf progradation (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). However, the onlap features observed above the Upper Miocene clinoform unit around Hz-1 well, are folded together with the prominent reflector on which they onlap (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Considering the data from the Hz-1 well, this unit is represented by an alternation of sandstone and marls, which are discordantly overlain by gravels at depth of 580 m (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e), that is coeval with the base of the Plio-Quaternary deposits. This folded discordance surface is folded and pinching out towards Strugača anticline to the N and eastern Medvednica Mt. to the S. As observed on seismic and surface structural data, the overlying Plio-Quaternary deposits are also folded and faulted (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). The next prominent syncline is the SE trending Lepoglava syncline located to the N of Ivanščica Mt. between two regional dextral faults, the Šoštanj fault to the S and Donat fault to the N (Figs.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e, \u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec11\" class=\"Section2\"\u003e \u003ch2\u003e3.2. Vitrinite Reflectance\u003c/h2\u003e \u003cp\u003eVitrinite reflectance (VR, %R\u003csub\u003eo\u003c/sub\u003e) was measured on isolated organic matter using Zeiss Axio Imager microscope equipped with MSP 210 microscope spectrometer (oil immersion) following standard procedures (Stach et al., \u003cspan citationid=\"CR118\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Taylor et al., \u003cspan citationid=\"CR123\" class=\"CitationRef\"\u003e1998\u003c/span\u003e). Firstly, total organic carbon content (TOC) was determined on selected samples (siltstones and mudstones of Cretaceous, Jurassic, and Triassic age). The TOC content was measured on Leco C744 carbon analyser. To remove carbonates samples were pre-treated with hot 18% HCl. Then, organic matter (kerogen) was isolated. Organic matter concentrate was obtained after standard HCl/HF/ZnCl\u003csub\u003e2\u003c/sub\u003e treatment of rock. Standards used for calibration were Spinel (0.426%R\u003csub\u003eo\u003c/sub\u003e), Sapphire (0.596%R\u003csub\u003eo\u003c/sub\u003e), Yttrium-Aluminum-Garnet (0.905%R\u003csub\u003eo\u003c/sub\u003e), Gadolinium-Gallium-Garnet (1.721%R\u003csub\u003eo\u003c/sub\u003e), Cubic-Zirconia (3.12%R\u003csub\u003eo\u003c/sub\u003e), Strontium-Titanate (5.38%R\u003csub\u003eo\u003c/sub\u003e). VR was converted to peak paleotemperatures using formulas defined by Barker \u0026amp; Pawlewicz (\u003cspan citationid=\"CR10\" class=\"CitationRef\"\u003e1994\u003c/span\u003e) for burial heating (T\u003csub\u003epeak\u003c/sub\u003e=(lnRr\u0026thinsp;+\u0026thinsp;1.68)/0.0124). Organic matter was examined on Olympus BX-51 microscope.\u003c/p\u003e \u003cp\u003eThe organic matter content in analysed siltstones and mudstones ranges from 0.16 to 1.16 wt. % TOC (Table\u0026nbsp;\u003cspan refid=\"Tab1\" class=\"InternalRef\"\u003e1\u003c/span\u003e). Generally, organic matter content is low (TOC\u0026thinsp;\u0026lt;\u0026thinsp;0,3%) except in Jurassic (GV-476) and Triassic (GT-240) siltstones (0,91 and 1,16% TOC, respectively). Organic matter is mainly fine detrital and of terrigenous origin, represented either with vitrinite macerals or with dark, non-fluorescent, highly thermally altered amorphous organic matter. Inertinite, mainly fusinite particles are evidenced as well.\u003c/p\u003e \u003cp\u003e \u003cdiv class=\"gridtable\"\u003e\u003ctable float=\"Yes\" id=\"Tab1\" border=\"1\"\u003e \u003ccaption language=\"En\"\u003e \u003cdiv class=\"CaptionNumber\"\u003eTable 1\u003c/div\u003e \u003cdiv class=\"CaptionContent\"\u003e \u003cp\u003e\u003cspan type=\"SmallCaps\" class=\"SmallCaps\" name=\"Emphasis\"\u003eVitrinite Reflectance Analytical Data\u003c/span\u003e\u003c/p\u003e \u003c/div\u003e \u003c/caption\u003e \u003ccolgroup cols=\"14\"\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c1\" colnum=\"1\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c2\" colnum=\"2\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c3\" colnum=\"3\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c4\" colnum=\"4\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c5\" colnum=\"5\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c6\" colnum=\"6\"\u003e\u003c/div\u003e \u003cdiv align=\"char\" char=\".\" class=\"colspec\" colname=\"c7\" colnum=\"7\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c8\" colnum=\"8\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c9\" colnum=\"9\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c10\" colnum=\"10\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c11\" colnum=\"11\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c12\" colnum=\"12\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c13\" colnum=\"13\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c14\" colnum=\"14\"\u003e\u003c/div\u003e \u003cthead\u003e \u003ctr\u003e \u003cth align=\"left\" colname=\"c1\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c2\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colspan=\"2\" nameend=\"c4\" namest=\"c3\"\u003e \u003cp\u003eCoordinates\u003c/p\u003e \u003c/th\u003e \u003cth align=\"left\" colname=\"c5\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c11\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c12\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c13\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c14\"\u003e\u0026nbsp;\u003c/th\u003e \u003c/tr\u003e \u003c/thead\u003e \u003ctbody\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eSample\u003c/p\u003e \u003cp\u003e(domain)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLithology\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003eLatitude\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003eLongitude\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003eTOC\u003csub\u003eLeco\u003c/sub\u003e(%)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003eVR\u003c/p\u003e \u003cp\u003e%R\u003csub\u003eo\u003c/sub\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e \u003cp\u003eNo.\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003eSD\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e%R\u003csub\u003emin\u003c/sub\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e%R\u003csub\u003emax\u003c/sub\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003eTAI\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003eConversion\u003c/p\u003e \u003cp\u003eTAI-%R\u003csub\u003eo\u003c/sub\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003eT\u003csub\u003epeak\u003c/sub\u003e\u003c/p\u003e \u003cp\u003e(⁰C)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003eRange T\u003csub\u003epeaK\u003c/sub\u003e \u003c/p\u003e \u003cp\u003e (⁰C)\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-224\u003c/p\u003e \u003cp\u003e(SDIP)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Cretaceous Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.174581\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.066425\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,31\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e2,10\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e35\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,27\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e1,63\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e2,57\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e2\u0026ndash;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e200\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e180\u0026ndash;220\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1416\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Cretaceous Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.163606\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.093678\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,16\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;230\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;230\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1633\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Cretaceous Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.162534\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.061793\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,22\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e2,19\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e24\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,21\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e1,80\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e2,54\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e2\u0026ndash;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e200\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e190\u0026ndash;220\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eDJI-8,30\u003c/p\u003e \u003cp\u003e(SDIP)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Cretaceous Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.175544\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.073502\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,20\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e2\u0026ndash;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;200\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e190\u0026ndash;220\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-476\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eJurassic Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.159107\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.096391\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,91\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e1,81\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e140\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,18\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e1,44\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e2,27\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e3\u003csup\u003e+\u003c/sup\u003e-4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e1,8\u0026thinsp;\u0026minus;\u0026thinsp;2,2\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e185\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e170\u0026ndash;200\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1257A\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eJurassic Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.156935\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.121706\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,27\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e2\u0026ndash;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;200\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;200\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1257B\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eJurassic Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.156935\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.121706\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,21\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e2\u0026ndash;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;200\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;200\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1477\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Jurassic Mudstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.172566\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.159687\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,19\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e2,93\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e7\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,30\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e2,45\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e3,26\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e2\u0026ndash;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e225\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e210\u0026ndash;230\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1585\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Jurassic Mudstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.174929\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.161486\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,24\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e1,86\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e5\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,07\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e1,76\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e1,95\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e3\u003csup\u003e+\u003c/sup\u003e-4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e1,8\u0026thinsp;\u0026minus;\u0026thinsp;2,2\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e190\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e180\u0026ndash;190\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eMR-24,50\u003c/p\u003e \u003cp\u003e(SDII)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Jurassic Mudstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.164998\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.135985\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,26\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e1,95\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e45\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,53\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e0,92\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e2,80\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e3\u003csup\u003e+\u003c/sup\u003e-4\u003csup\u003e\u0026minus;\u003c/sup\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e1,8\u0026thinsp;\u0026minus;\u0026thinsp;2,2\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e190\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e135\u0026ndash;220\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-113\u003c/p\u003e \u003cp\u003e(SDIP)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eMiddle Triassic Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.192836\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e15.98391\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e0,40\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;230\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;230\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGT-240\u003c/p\u003e \u003cp\u003e(SDIP)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eMiddle Triassic Siltstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.181091\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.196046\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e1,16\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e3,84\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"char\" char=\".\" colname=\"c7\"\u003e \u003cp\u003e31\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e0,42\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e3,05\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e4,71\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e4\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e\u0026gt;\u0026thinsp;3\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e245\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e220\u0026ndash;260\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003c/tbody\u003e \u003c/colgroup\u003e \u003ctfoot\u003e \u003ctr\u003e\u003ctd colspan=\"14\"\u003eThe data are discussed in the text. Abbreviations: TOC\u0026thinsp;=\u0026thinsp;total organic carbon; VR\u0026thinsp;=\u0026thinsp;vitrinite reflectance; No\u0026thinsp;=\u0026thinsp;number of measurements; SD\u0026thinsp;=\u0026thinsp;standard deviation; R\u003csub\u003emin\u003c/sub\u003e = minimum vitrinite reflectance; R\u003csub\u003emax\u003c/sub\u003e = maximum vitrinite reflectance; TAI\u0026thinsp;=\u0026thinsp;thermal alteration index; SDII\u0026thinsp;=\u0026thinsp;structural domain Ivanščica imbricates; SDIP\u0026thinsp;=\u0026thinsp;structural domain Ivanščica parautochton; o.m. = ophiolitic m\u0026eacute;lange.\u003c/td\u003e\u003c/tr\u003e \u003c/tfoot\u003e \u003c/table\u003e\u003c/div\u003e \u003c/p\u003e \u003cp\u003eMiddle Triassic organic matter is highly thermally altered. VR (3,84%R\u003csub\u003eo\u003c/sub\u003e) correspond to paleo-temperatures of \u0026ge;\u0026thinsp;245 ⁰C (Bostick, \u003cspan citationid=\"CR17\" class=\"CitationRef\"\u003e1979\u003c/span\u003e; Barker \u0026amp; Pawlewicz, \u003cspan citationid=\"CR10\" class=\"CitationRef\"\u003e1994\u003c/span\u003e; Rainer et al., \u003cspan citationid=\"CR90\" class=\"CitationRef\"\u003e2016\u003c/span\u003e). Organic matter in Lower Jurassic mudstones is mainly amorphous while in Jurassic siltstones vitrinite macerals prevailed. VR and TAI in all Jurassic samples indicate transition from catagenesis into metagenesis except in GV-1477 sample. VR in GV-1477 is higher (2.93%Ro) than in two others measured (1,86 and 195, respectively) pointing to higher paleotemperatures (\u0026gt;\u0026thinsp;225 ⁰C) in that sample in relation to other ones (\u0026asymp;\u0026thinsp;190 ⁰C). According to VR and TAI Lower Cretaceous siltstones have reached onset of metagenesis. VR is slightly higher than 2%R\u003csub\u003eo\u003c/sub\u003e indicating paleotemperatures\u0026thinsp;\u0026ge;\u0026thinsp;200 ⁰C.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec12\" class=\"Section2\"\u003e \u003ch2\u003e3.3. Apatite Fission Track\u003c/h2\u003e \u003cp\u003eApatite fission track (AFT) analyses was carried out by Institute of Geology at Czech Academy of Sciences. Samples for AFT analysis were collected from both Permo-Mesozoic structural domains to compare their thermal histories and reconstruct the uplift path of the Alpine \u0026ndash; Dinaridic transitional zone. Since the study area consists mostly of carbonate sedimentary rocks and thus lacking apatite-rich lithologies, we selected the only three potentially suitable lithostratigraphic units for apatite extraction. Among overall eight samples collected from Permian to Lower Triassic sandstones, Middle Triassic volcanic rocks and Lower Cretaceous turbidites, only three samples from Permian to Lower Triassic sandstones gave enough apatites for analysis and only two of them (GV-1609 and GV-1625; Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e) were successfully analysed. The apatites extraction from the rock samples (8 kg per sample) was done following standard mineral separation (REF) and their preparation for counting and subsequent measurement of uranium content by using LA-ICP-MS (Laser Ablation Inductively Coupled Plasma Mass Spectrometry) following the procedure and age calculation described by Hasebe et al. (\u003cspan citationid=\"CR50\" class=\"CitationRef\"\u003e2004\u003c/span\u003e). IsoplotR software (Vermeesch, \u003cspan citationid=\"CR135\" class=\"CitationRef\"\u003e2018\u003c/span\u003e) and Durango apatite standard were used for zeta factor calculation and final calculation of ages.\u003c/p\u003e \u003cp\u003eThe results of two AFT analyses are presented in Table\u0026nbsp;\u003cspan refid=\"Tab2\" class=\"InternalRef\"\u003e2\u003c/span\u003e. Two analysed detrital samples from the SDIP yield a central age of 56.36\u0026thinsp;\u0026plusmn;\u0026thinsp;2.50 Ma for GV-1609 and 67.27\u0026thinsp;\u0026plusmn;\u0026thinsp;5.38 Ma for GV-1625 (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Measured mean track length is 11.12\u0026thinsp;\u0026plusmn;\u0026thinsp;2.54 \u0026micro;m for the sample GV-1609 and 11.76\u0026thinsp;\u0026plusmn;\u0026thinsp;1.76 \u0026micro;m for the sample GV-1625. The AFT age and length measurements were combined with paleo temperature and stratigraphic constraints in order to derive the cooling trajectories for both samples by using HeFTy software based on fission track annealing algorithms (Ketcham, \u003cspan citationid=\"CR55\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Ketcham et al., \u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2007\u003c/span\u003e). The obtained time-temperature model of both samples (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e) indicates fast, tectonically induced cooling that took place immediately after peak temperature conditions that were reached in the Early Cretaceous (ca. 140 Ma). Model suggests a drop of a temperature from a minimum 300 ⁰C to 100 ⁰C between 140 and 125 Ma and a cooling rate of a minimum 13.33 ⁰C/Ma. This implies denudation rate of 0.53 km/Ma if assume an average thermal gradient of 25 ⁰C/km. The length of the apatite fission tracks corrected for the angle of measurement indicate subsequent relatively slow cooling period through the apatite partial annealing zone (APAZ) and following stable period with only minor fluctuations around the lower temperature limit of the APAZ (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003cdiv class=\"gridtable\"\u003e\u003ctable float=\"Yes\" id=\"Tab2\" border=\"1\"\u003e \u003ccaption language=\"En\"\u003e \u003cdiv class=\"CaptionNumber\"\u003eTable 2\u003c/div\u003e \u003cdiv class=\"CaptionContent\"\u003e \u003cp\u003eApatite Fission Track Analytical Data\u003c/p\u003e \u003c/div\u003e \u003c/caption\u003e \u003ccolgroup cols=\"16\"\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c1\" colnum=\"1\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c2\" colnum=\"2\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c3\" colnum=\"3\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c4\" colnum=\"4\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c5\" colnum=\"5\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c6\" colnum=\"6\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c7\" colnum=\"7\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c8\" colnum=\"8\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c9\" colnum=\"9\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c10\" colnum=\"10\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c11\" colnum=\"11\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c12\" colnum=\"12\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c13\" colnum=\"13\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c14\" colnum=\"14\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c15\" colnum=\"15\"\u003e\u003c/div\u003e \u003cdiv align=\"left\" class=\"colspec\" colname=\"c16\" colnum=\"16\"\u003e\u003c/div\u003e \u003cthead\u003e \u003ctr\u003e \u003cth align=\"left\" colname=\"c1\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c2\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colspan=\"2\" nameend=\"c4\" namest=\"c3\"\u003e \u003cp\u003eCoordinates\u003c/p\u003e \u003c/th\u003e \u003cth align=\"left\" colname=\"c5\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c6\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c7\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c8\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c9\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c10\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c11\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c12\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c13\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c14\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c15\"\u003e\u0026nbsp;\u003c/th\u003e \u003cth align=\"left\" colname=\"c16\"\u003e\u0026nbsp;\u003c/th\u003e \u003c/tr\u003e \u003c/thead\u003e \u003ctbody\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eSample\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLithology\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003eLatitude\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003eLongitude\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003eCentral age\u003c/p\u003e \u003cp\u003e(Ma\u0026nbsp;\u0026plusmn;\u0026nbsp;1σ)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003eN\u003csub\u003eGr\u003c/sub\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e \u003cp\u003eρ\u003csub\u003es\u003c/sub\u003e (N\u003csub\u003eS\u003c/sub\u003e)\u003c/p\u003e \u003cp\u003e(10\u003csup\u003e5\u003c/sup\u003e\u0026nbsp;cm\u003csup\u003e\u0026minus;\u0026thinsp;2\u003c/sup\u003e)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e\u003csup\u003e238\u003c/sup\u003eU\u003c/p\u003e \u003cp\u003e(ppm)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e2σ\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003eMSWD\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003eP(χ2)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003eDisp.\u003c/p\u003e \u003cp\u003e(%)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003ePooled age (Ma \u0026plusmn;\u0026nbsp;1σ)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003eMTL \u003c/p\u003e \u003cp\u003e(\u0026micro;m\u0026thinsp;\u0026plusmn;\u0026thinsp;SD\u003csub\u003eL\u003c/sub\u003e)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c15\"\u003e \u003cp\u003eN\u003csub\u003eL\u003c/sub\u003e\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c16\"\u003e \u003cp\u003eD\u003csub\u003epar\u003c/sub\u003e\u003c/p\u003e \u003cp\u003e(\u0026micro;m)\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1609\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eUpper Permian sandstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.20068\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.08756\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e56.36\u0026thinsp;\u0026plusmn;\u0026thinsp;2.5\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e63\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e \u003cp\u003e0.09 (3396)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e21.50\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e1.03\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e5.5\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e0\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e28.43\u0026thinsp;\u0026plusmn;\u0026thinsp;3.54\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e\u0026nbsp;\u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e11.12\u0026thinsp;\u0026plusmn;\u0026thinsp;2.54\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c15\"\u003e \u003cp\u003e40\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c16\"\u003e \u003cp\u003e1.90\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003ctr\u003e \u003ctd align=\"left\" colname=\"c1\"\u003e \u003cp\u003eGV-1625\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c2\"\u003e \u003cp\u003eLower Triassic sandstone\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c3\"\u003e \u003cp\u003e46.20293\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c4\"\u003e \u003cp\u003e16.06070\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c5\"\u003e \u003cp\u003e67.27\u0026thinsp;\u0026plusmn;\u0026thinsp;5.38\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c6\"\u003e \u003cp\u003e39\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c7\"\u003e \u003cp\u003e0.24 (1788)\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c8\"\u003e \u003cp\u003e26.90\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c9\"\u003e \u003cp\u003e0.99\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c10\"\u003e \u003cp\u003e7\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c11\"\u003e \u003cp\u003e0\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c12\"\u003e \u003cp\u003e42.29\u0026thinsp;\u0026plusmn;\u0026thinsp;6.19\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c13\"\u003e \u003cp\u003e56.2 \u0026plusmn;\u0026nbsp;8.5\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c14\"\u003e \u003cp\u003e11,76\u0026thinsp;\u0026plusmn;\u0026thinsp;1.76\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c15\"\u003e \u003cp\u003e37\u003c/p\u003e \u003c/td\u003e \u003ctd align=\"left\" colname=\"c16\"\u003e \u003cp\u003e1.74\u003c/p\u003e \u003c/td\u003e \u003c/tr\u003e \u003c/tbody\u003e \u003c/colgroup\u003e \u003ctfoot\u003e \u003ctr\u003e\u003ctd colspan=\"16\"\u003eThe data presented in table are discussed in the text, see also Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e. Abbreviations: N\u003csub\u003eGr\u003c/sub\u003e = number of dated apatite crystals; ρ\u003csub\u003es\u003c/sub\u003e\u0026thinsp;=\u0026thinsp;spontaneous track densities; N\u003csub\u003eS\u003c/sub\u003e = sum of spontaneous fission-tracks; \u003csup\u003e238\u003c/sup\u003eU = mean \u003csup\u003e238\u003c/sup\u003eU content value; MSWD\u0026thinsp;=\u0026thinsp;mean square of weighted deviates; P(χ2)\u0026thinsp;=\u0026thinsp;probability of obtaining chi-square (χ2) for n degrees of freedom (n is the number of crystals); Disp. = dispersion in single-grain ages; MTL\u0026thinsp;=\u0026thinsp;C axis projected mean track length with \u0026plusmn;\u0026thinsp;the standard deviation (SD\u003csub\u003eL\u003c/sub\u003e); N\u003csub\u003eL\u003c/sub\u003e = number of measured confined tracks; D\u003csub\u003epar\u003c/sub\u003e = average etch pit diameter.\u003c/td\u003e\u003c/tr\u003e \u003c/tfoot\u003e \u003c/table\u003e\u003c/div\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e"},{"header":"4. Discussion","content":"\u003cdiv id=\"Sec14\" class=\"Section2\"\u003e \u003ch2\u003e4.1. Tectonic evolution of the study area and correlation with the Dinarides and the Alps\u003c/h2\u003e \u003cp\u003eIntegration of structural, AFT and VR data, together with the existing sedimentological and biostratigraphic data, enabled reconstruction of the five deformational events that affected Permo-Mesozoic and/or Cenozoic formations of Ivanščica Mt. In addition, based on lithostratigraphic characteristics of volcano-sedimentary successions and their superposition, two older Mesozoic extensional events are also supposed. These events are discussed below in the context of the tectonic evolution of Ivanščica Mt. and in the context of tectonic evolution of the Dinarides and Southern-Eastern Alps. The chronology of deformational events was partly derived from overprinting relations between documented deformational structures and partly based on new biostratigraphic ages of Mesozoic successions (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e) considered as pre-, syn- and post-tectonic deposits with respect to particular deformational events. Additional time constraints were established based on AFT data.\u003c/p\u003e \u003cdiv id=\"Sec15\" class=\"Section3\"\u003e \u003ch2\u003e4.1.1. Pre-Cretaceous tectonic evolution\u003c/h2\u003e \u003cp\u003eThe oldest deformational event (D1) on Ivanščica Mt., although not directly confirmed by deformational structures, is proposed here due to the presence of syn-rift volcano-sedimentary successions of Middle Triassic age. Namely, Anisian to Ladinian pelagic successions documented in the structural domain SDIP (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e), are interpreted as deposited in a relatively deep depocenters arranged in a form of half-grabens controlled by steep normal faults (Goričan et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Slovenec et al., \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e2020\u003c/span\u003e, \u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e2023\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). On Ivanščica Mt., the oldest pelagic deposits are Illyrian radiolarian cherts (Goričan et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Slovenec et al., \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Kukoč et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e), while on nearby Kuna gora Mt. ammonites dating of pelagic limestones indicate their Pelsonian age (Kukoč et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). Thus, this oldest deformational event (D1) is assumed as extensional and related with the opening of the Neotethys Ocean during Middle Triassic times. These half-graben depocenters were short-lived, and a shallow-marine carbonate sedimentation was re-established again in the Late Ladinian (Šimunić \u0026amp; Šimunić, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Goričan et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2005\u003c/span\u003e). Anisian-Ladinian extensional event is well-documented throughout the Alps and the Dinarides, characterized by deposition of coeval and lithologically similar volcano-sedimentary successions (for correlation, see Kukoč et al. \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2023\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eDuring Early Jurassic, after a period of Late Triassic shallow-marine sedimentation proved by Upper Triassic carbonates found in both pre-Oligocene structural domains of Ivanščica Mt. (i.e., in SDIP and SDII domains), a dramatic change in depositional environments took place. In the SDIP, deposition of shallow-marine carbonates continued from Late Triassic into Early Jurassic until the Pliensbachian. In contrast, in the SDII the Upper Triassic shallow-marine carbonates are covered by Lower Jurassic pelagic deposits. This dramatic deepening of depositional environments is assumed as related to yet another extensional event of Early Jurassic age (D2). As SDIP and SDII domains are separated by the ČMT (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003e and \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e), this NW-verging thrust (recent orientation) is likely an inverted Early Jurassic normal fault. However, since Pliensbachian, pelagic conditions prevailed in both structural domains (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). This Early Jurassic extensional event correlates well with Jurassic rifting recorded in the Dinarides (reference) and in the Southern and Eastern Alps, where similar lithostratigraphic successions are documented in (e.g. Bohm, 2003; Goričan et. al \u003cspan citationid=\"CR44\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Rožič et al. \u003cspan citationid=\"CR93\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). There, this Early Jurassic extension led to formation of the Alpine Tethys passive continental margin (e.g., Froitzheim \u0026amp; Eberli, \u003cspan citationid=\"CR39\" class=\"CitationRef\"\u003e1990\u003c/span\u003e; Froitzheim \u0026amp; Manatschal, \u003cspan citationid=\"CR38\" class=\"CitationRef\"\u003e1996\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec16\" class=\"Section3\"\u003e \u003ch2\u003e4.1.2. Early Cretaceous tectonic evolution\u003c/h2\u003e \u003cp\u003eTectonic emplacement of the Repno Complex over the stratigraphic succession of the Adriatic continental passive margin recorded in the SDII (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e) marks the oldest contractional event recorded on Ivanščica Mt. (D3). The age constraint for this event on Ivanščica Mt. is provided by the youngest formation directly overthrusted by the Repno Complex, which is uppermost Tithonian to Valanginian Aptychus limestone (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). This indicates that the D3 event occurred during the Valanginian or slightly earlier.\u003c/p\u003e \u003cp\u003eThe peak temperature conditions of approximately 200\u0026deg;C recorded in the passive margin successions within the SDII (Table\u0026nbsp;\u003cspan refid=\"Tab1\" class=\"InternalRef\"\u003e1\u003c/span\u003e) were likely reached during this event. The obtained temperatures, calculated using the vitrinite reflection method, are only slightly higher than those estimated from the colour of pollen and dinoflagellate cysts obtained from the Repno Complex (Babić et al. \u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e2002\u003c/span\u003e). This is in line with the structurally higher position of the Repno Complex with respect to the underlying passive margin successions.\u003c/p\u003e \u003cp\u003eLate Jurassic to earliest Cretaceous obduction of the Neotethyan ophiolites on the eastern continental margin of Adria is well documented throughout the Dinarides and the Hellenides (e.g., Bortolotti et al., \u003cspan citationid=\"CR16\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Tremblay et al., \u003cspan citationid=\"CR128\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Nirta et al., \u003cspan citationid=\"CR77\" class=\"CitationRef\"\u003e2018\u003c/span\u003e with references). It is proposed that this obduction is responsible for a low-grade metamorphic overprint recorded in Paleo-Mesozoic units of the distal Adriatic margin underlaying the ophiolites (e.g., Tomljenović et al., \u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Porkolab et al. \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Mišur et al., \u003cspan citationid=\"CR73\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). On Medvednica Mt., monazite dating indicate Berriasian metamorphic event (~\u0026thinsp;143 Ma; Mišur et al. \u003cspan citationid=\"CR73\" class=\"CitationRef\"\u003e2023\u003c/span\u003e), while in the central Dinarides, K/Ar ages indicate Tithonian to Valanginian age of this metamorphic overprint (150\u0026ndash;135 Ma; Porkolab et al. \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). Therefore, Valanginian age assumed for the D3 deformational event on Ivanščica Mt. is only slightly younger than these metamorphic ages. However, as Permian to Lower Cretaceous formations of Ivanščica Mt. are not affected by this metamorphic overprint but only a minor thermal alteration, at the time of the obduction they were in a more external (i.e., continentward) paleogeographic position on the Adriatic margin than units affected by this metamorphism. In the central Dinarides, the youngest deposits directly overthrusted by the Neotethyan ophiolites and ophiolitic m\u0026eacute;lange have so far been described from the East Bosnian-Durmitor thrust sheet where the ophiolitic m\u0026eacute;lange is found in a tectonic position above Tithonian to Berriasian pelagic limestone (Vishnevskaya et al., \u003cspan citationid=\"CR136\" class=\"CitationRef\"\u003e2009\u003c/span\u003e). This limestone is correlative to the Apthychus Limestone from Ivanščica, although its age is constrained within a shorter stratigraphic range. Middle Triassic to Lower Cretaceous succession exposed on Ivanščica Mt. and attributed to the Adriatic continental margin correlates well with contemporaneous successions described from the Pre-Karst zone of the central Dinarides (Vukovski et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2023\u003c/span\u003e with references).\u003c/p\u003e \u003cp\u003ePopulation of detrital zircons from the Oštrc Fm. with an Early Cretaceous cooling ages (ca. 145\u0026thinsp;\u0026minus;\u0026thinsp;134 Ma; Lužar-Oberiter et al., \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2012\u003c/span\u003e) was sourced from these more internal units (e.g. Medvednica Mt.), where zircons were reset due to obduction (D3) and exhumed during subsequent D4 event.\u003c/p\u003e \u003cp\u003eThe following contractional event recorded by deformational structures documented in the SDII and SDIP of Ivanščica Mt. is here assigned as D4 event. It resulted in formation of contractional structures observed at different scales of observation. These include NW-vergent imbricates of the SDII, which comprise Upper Triassic and Jurassic Adriatic passive margin succession together with the overlying Repno Complex (Figs.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e, \u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e10\u003c/span\u003e). NW-ward directed thrusting of the SDII over the SDIP along the ČMT (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e), the formation of the BZBT (Figs.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e, \u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003eh), NW-ward reverse faulting in the SDIP (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e) and intense pervasive folding of non-competent Jurassic to Early Cretaceous pelagic deposits within both structural domains are also attributed to this deformational event (Figs.\u0026nbsp;\u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003ea-f). Sedimentological evidence supports a late Early Cretaceous age of this contractional event. The youngest deposits affected by this event are turbidites of Hauterivian to Albian Oštrc Fm., thus indicating that this event should be at least partly post Albian in age. However, as the Oštrc Fm. contains lithoclasts of the underlying latest Tithonian to Valanginian Aptychus limestone (Zupanič et al., \u003cspan citationid=\"CR146\" class=\"CitationRef\"\u003e1981\u003c/span\u003e), we consider this formation as syntectonic with respect to D4 deformational event. In addition to lithoclasts of the Aptychus limestone, the Oštrc Fm. contains other shallow-marine to pelagic lithoclasts of Triassic-Jurassic age, as well as mafic volcanic lithoclasts and abundant Cr-spinel grains (Zupanič et al., \u003cspan citationid=\"CR146\" class=\"CitationRef\"\u003e1981\u003c/span\u003e). The source of all these lithoclasts and Cr-spinels is seen in the imbricates of the SDII. This indicates a strong, tectonically induced, fast synsedimentary Hauterivian to Albian exhumation and erosion of the uppermost Triassic to lowermost Cretaceous Adria passive margin succession together with tectonically overlaying Repno complex. This is in accordance with our AFT time-temperature models (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003e) suggesting fast tectonically induced Early Cretaceous cooling and exhumation. The upper age limit of D4 event cannot be precisely constrained on Ivanščica Mt. due to the lack of post-tectonic cover deposits older than Oligocene. However, on the neighbouring Medvednica Mt. correlative deformational event, D1 of van Gelder et al. (\u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) or D2 of Tomljenović et al. (\u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2008\u003c/span\u003e), predates the Late Cretaceous transgression and deposition of the Gosau-type sediments (Glog Fm.; Lužar-Oberiter et al., \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2012\u003c/span\u003e with references). Considering an Oligocene-earliest Miocene c. 130\u0026deg; rotation of the block carrying Medvednica and neighbouring northern Croatian mountains (including Ivanščica) proposed by Tomljenović et al. (\u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2008\u003c/span\u003e), the original trend of the D4 deformational structures documented on Ivanščica would be NW-SE and with SW-ward direction of tectonic transport. In that case, the initial pre-Miocene orientation and vergence of the D4 structures on Ivanščica Mt. would correspond well with contemporaneous and commonly observed SW verging structures in the Internal Dinarides (e.g., Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Schefer, \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Porkolab et al., \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2019\u003c/span\u003e, Nirta et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe thermal alterations recorded in Mesozoic sediments of the SDIP likely reflect D4 deformational event, since unlike the SDII, the SDIP was not overthrusted by an ophiolite nappe. Instead, continuous sedimentation of the Oštrc Fm. on top of the Aptychus limestone is recorded in the SDIP (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). Therefore, we propose that peak temperature conditions in the SDIP were reached during D4 thrusting of the SDII over the SDIP, soon followed by the exhumation and cooling due to propagation of this thrusting towards the Adriatic foreland. In-sequence D4 thrusting is supported by the presence of the syn-tectonic Oštrc Fm. exclusively found in the leading sector of the SDII imbricate fan (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e and \u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e10\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eIn the central Internal Dinarides, contractional deformational event correlative with the D4 documented on Ivanščica postdates the ophiolite obduction and predates the deposition of Upper Cretaceous \u0026lsquo;overstepping\u0026rsquo; sequences (see in Nirta et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Here, this event is manifested in SW-ward nappe stacking, exhumation, erosion and redeposition of passive margin units of the distal Adriatic margin together with overlaying ophiolitic units (Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Schefer \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Tremblay et al., \u003cspan citationid=\"CR128\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Porkolab et al., \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Nirta et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e), also affecting the syn-orogenic turbiditic Vranduk Fm. and its proximal equivalent the Pogari Fm. (Mikes et al., \u003cspan citationid=\"CR70\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Nirta et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). These formations are corelative with syn-orogenic Hauterivian to Albian Oštrc Fm. and Aptian\u0026ndash;Albian shallow-water Bistra Fm. (Gušić, \u003cspan citationid=\"CR45\" class=\"CitationRef\"\u003e1975\u003c/span\u003e; Crnjaković, \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1989\u003c/span\u003e; Lužar-Oberiter et al., \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2012\u003c/span\u003e) unconformably overlying the Repno Complex in Medvednica Mt. Still, Oštrc and Bistra formations are younger than the Vranduk and Pogari formations (Mikes et al., \u003cspan citationid=\"CR70\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Nirta et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e with references therein; Hrvatović, \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2022\u003c/span\u003e), thus suggesting younger age of D4 deformations and more forelandward position of Ivanščica Mt. during this event.\u003c/p\u003e \u003cp\u003eIn the Eastern Alps, Early Cretaceous contractional deformational event correlative with D4 event of Ivanščica is well-known as Eo-Alpine event characterized by WNW-ward stacking of the Austroalpine nappe units (Neubauer et al., \u003cspan citationid=\"CR75\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e, \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e and references therein) and a deposition of the syn-orogenic Rossfeld Formation of a Late Valanginian to Aptian age (~\u0026thinsp;135\u0026thinsp;\u0026minus;\u0026thinsp;110 Ma; Faupl \u0026amp; Wagreich, \u003cspan citationid=\"CR34\" class=\"CitationRef\"\u003e2000\u003c/span\u003e). Moreover, regional Early Cretaceous event is documented along whole East Alpine-Dinaridic-Hellenic belt (Neubauer et al., \u003cspan citationid=\"CR75\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Schefer, \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Bortolotti et al., \u003cspan citationid=\"CR16\" class=\"CitationRef\"\u003e2013\u003c/span\u003e), including Wester Carpathians (Plašienka et al., \u003cspan citationid=\"CR86\" class=\"CitationRef\"\u003e1997a\u003c/span\u003e, \u003cspan citationid=\"CR87\" class=\"CitationRef\"\u003eb\u003c/span\u003e). In general, it is interpreted as related to the closure of the northern branch of the Neotethys Ocean (Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Nirta et al., \u003cspan citationid=\"CR77\" class=\"CitationRef\"\u003e2018\u003c/span\u003e, \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe D4 event resulted with a regional emersion recorded on Ivanščica Mt. as well as throughout the Dinarides and the Eastern Alps. The oldest sediments covering Mesozoic formations on Ivanščica Mt. are lowermost Miocene clastic deposits found on the southern slopes (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). Locally across the Dinarides, this emersion was considerably shorter and lasted until the Late Cretaceous when \u0026lsquo;overstepping sediments\u0026rsquo; were deposited on top of Mesozoic formations (Nirta et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Hrvatović, \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2022\u003c/span\u003e). Similarly, in the Medvednica Mt. these sediments are known as Gosau-type deposits and are of Santonian to Paleocene age (Crnjaković, \u003cspan citationid=\"CR25\" class=\"CitationRef\"\u003e1979\u003c/span\u003e). Additionally, lateritic sediments on top of serpentinites are found at the base of Campanian rudist limestone (Palinkaš et al., \u003cspan citationid=\"CR78\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Moro et al., \u003cspan citationid=\"CR74\" class=\"CitationRef\"\u003e2010\u003c/span\u003e). Another evidence of emersion can be found in bauxite deposits on the neighbouring Ravna gora Mt. formed on top of Triassic dolomites, likely exhumed during the D4 event. Bauxites are sealed by Middle and Upper Eocene foraminiferal limestone (Šimunić et al., \u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1981\u003c/span\u003e; Šimunić, \u003cspan citationid=\"CR105\" class=\"CitationRef\"\u003e1992\u003c/span\u003e). Post Early Cretaceous emersion in the study area suggests that Late Cretaceous to Eocene sedimentary burial cannot be the explanation for the thermal alteration, as it is interpreted for the area of Sava folds and further westward in Slovenian Basin where continuous latest Cretaceous to Middle Eocene sedimentation resulted in deposition of at least 5 km of flysch type sediments (Rainer et al., \u003cspan citationid=\"CR90\" class=\"CitationRef\"\u003e2016\u003c/span\u003e). Records of this emersion, which lasted from latest Jurassic \u0026ndash; earliest Cretaceous until the Late Turonian transgression and the deposition of the Lower Gosau Group are found in the Austroalpine unit and the Western Carpathians (Wagreich \u0026amp; Faupl, \u003cspan citationid=\"CR139\" class=\"CitationRef\"\u003e1994\u003c/span\u003e; Wagreich \u0026amp; Marschalko, \u003cspan citationid=\"CR140\" class=\"CitationRef\"\u003e1995\u003c/span\u003e; Stern \u0026amp; Wagreich; \u003cspan citationid=\"CR122\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Steiner et al., \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e2021\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe cooling trajectories of AFT samples obtained in this study indicate a tectonically stable period with only minor fluctuations after the fast cooling related to the D4 event (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003e). Obtained central ages of 56.4\u0026thinsp;\u0026plusmn;\u0026thinsp;2.5 Ma for sample GV-1609 and 67.3\u0026thinsp;\u0026plusmn;\u0026thinsp;5.4 Ma for sample GV-1625 are result of a long-lasting stay of these samples around the lower limit of the APAZ (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003e). For that reason, we suppose that the SDIP and the SDII were not affected by any major deformation postdating D4 Early Cretaceous contraction and predating D5 Early Miocene extension.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec17\" class=\"Section3\"\u003e \u003ch2\u003e4.1.3. Neogene-recent tectonic evolution\u003c/h2\u003e \u003cp\u003eNE dipping low angle listric normal growth faults documented on reflection seismic sections (Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e), associated with ENE striking dextral strike-slip faults around the prominent Early Miocene syn-rift depocenters N of Ivanščica Mt. (Figs.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec, \u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e) are attributed to the D5 deformational event that resulted with Early Miocene NE-SW directed extension. The D5 normal faults crosscut older structures (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e) with only sporadic evidence for their later inversion or reactivation. Termination of D5 extension is marked by the Late Badenian transgression and deposition of clastic to carbonate sediments, which seal Early Miocene rift structures (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). The termination of this event corresponds with a gradual decrease in volcanic activity during late Middle Miocene in the Pannonian basin (Bal\u0026aacute;zs et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Pavelić \u0026amp; Kovačić, \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). Onlapping of Pannonian over Sarmatian sediments indicate a Late Sarmatian short-lived contraction (D6), also documented in reflection seismic sections near Medvednica Mt. by Tomljenović \u0026amp; Csontos (\u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e). It resulted in partly reactivation of the D5 normal listric faults into reverse faults (Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e). The subsequent stage of thermal subsidence well documented across the entire Pannonian basin area was characterised by filling of accommodation space and gradual filling of the basin during Late Miocene and Pliocene times (Kovačić et al., \u003cspan citationid=\"CR58\" class=\"CitationRef\"\u003e2004\u003c/span\u003e; Sebe et al., \u003cspan citationid=\"CR101\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe youngest deformation event (D7) is constrained to Late Miocene to present, characterized by NNW-SSE contraction. To the north of Ivanščica Mt., this contraction is accommodated by the reactivation of ENE striking dextral faults (e.g. Šoštanj fault; Fig.\u0026nbsp;\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003ed, e) and by formation of E to NE trending km large folds and SE striking dextral faults (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). Here, reverse faulting is mostly accommodated along local transpressional ramps of major strike-slip faults. The influence of strike-slip faulting diminishes sharply to the south at the N to NW vergent Northern Ivanščica reverse fault (Figs.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e, \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e), which possibly represents Early Cretaceous D4 fault reactivated during D7 Late Miocene-present contraction. This fault is responsible for NW-ward high angle thrusting of the Permo\u0026ndash;Mesozoic units of the SDIP and passively transported SDII over Upper Oligocene to Lower Miocene deposits, inclination of homoclinal S to SE dipping Miocene strata in the southern slopes of the mountain (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e), and final uplift of Ivanščica. SE striking Gotalovec \u0026ndash; Prigorec dextral fault is attributed to D7 event according to Late Pannonian age of deformed strata. To the south towards Medvednica Mt., same NNW-SSE contraction resulted in formation of series of E to NE trending, tens kilometres long anticlines and synclines, with small offset reverse faults developed in the limbs of anticlines (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Onlapping and thinning of syn-tectonic strata along the flanks of anticlines indicate that the main stage of folding started in the late Pannonian (Figs.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003e, \u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). This deformation and timing corelates well with previous field kinematic studies and interpretations of seismic data from wider study area (Placer, \u003cspan citationid=\"CR85\" class=\"CitationRef\"\u003e1999b\u003c/span\u003e; Tomljenović \u0026amp; Csontos, \u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Bal\u0026aacute;zs et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2016\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec18\" class=\"Section2\"\u003e \u003ch2\u003e4.2. Tectonic position of Ivanščica Mt.\u003c/h2\u003e \u003cp\u003eEarlier studies considered Ivanščica, for the most part, as a S-vergent Neogene nappe of the South Alpine unit, thrusted over the ophiolitic m\u0026eacute;lange of the Western Vardar ophiolitic unit of the Dinarides (Repno complex; Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec; Placer, \u003cspan citationid=\"CR84\" class=\"CitationRef\"\u003e1999a\u003c/span\u003e; Schmid et al., \u003cspan citationid=\"CR96\" class=\"CitationRef\"\u003e2008\u003c/span\u003e, \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; van Gelder et al., \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e). Our investigation did not reveal any S to SE vergent thrust of the Miocene age. The only SE vergent fault is the BZBT, whose location and kinematics coincides with the frontal thrust of the South Alpine unit according to Placer, (\u003cspan citationid=\"CR84\" class=\"CitationRef\"\u003e1999a\u003c/span\u003e), van Gelder et al. (\u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) and Schmid et al. (\u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). However, BZBT is sealed by Upper Oligocene and Miocene deposits (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e) and thus predates Oligocene\u0026ndash;earliest Miocene rotation. Furthermore, we interpret the BZBT to be Early Cretaceous in age. Therefore, the initial top-NE vergence of the BZBT and its Early Cretaceous age oppose the interpretation about SE-ward Miocene thrust. In addition, the main shortening phase in the South Alpine unit (the Valsugana phase, ca. 14\u0026thinsp;\u0026minus;\u0026thinsp;8 Ma, Castelarin et al., 1992; Doglioni, \u003cspan citationid=\"CR27\" class=\"CitationRef\"\u003e1992\u003c/span\u003e; Castellarin \u0026amp; Canteli, \u003cspan citationid=\"CR20\" class=\"CitationRef\"\u003e2000\u003c/span\u003e; Zattin et al., \u003cspan citationid=\"CR145\" class=\"CitationRef\"\u003e2003\u003c/span\u003e, \u003cspan citationid=\"CR144\" class=\"CitationRef\"\u003e2006\u003c/span\u003e), was coeval with the regional transgression and the deposition of shallow-water to pelagic sediments in the study area, including whole Pannonian Basin (Pavelić \u0026amp; Kovačić, \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2018\u003c/span\u003e and references therein). However, the same driving process which caused thrusting within the South Alpine unit, the indentation and CCW rotation of Adria, is responsible for the Late Pannonian (~\u0026thinsp;6 Ma) to recent contraction (D7). In the area of the Dinarides and the Pannonian Basin, this contraction resulted in folding, reverse and strike-slip faulting (Tomljenović \u0026amp; Csontos, \u003cspan citationid=\"CR126\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; Bal\u0026aacute;zs et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; van Unen et al., \u003cspan citationid=\"CR133\" class=\"CitationRef\"\u003e2019a\u003c/span\u003e, \u003cspan citationid=\"CR134\" class=\"CitationRef\"\u003eb\u003c/span\u003e). Contrary, at the same time the South Alpine unit was characterised by thrusting (Castelarin et al., 1992; Picotti et al., \u003cspan citationid=\"CR83\" class=\"CitationRef\"\u003e2022\u003c/span\u003e). Hence, in contrast to the previous studies, our data suggests that the study area was not affected by the Miocene S-ward retro wedge thrusting of the South Alpine unit. Considering Mesozoic and Cenozoic tectono-sedimentary evolution of Ivanščica Mt. as described earlier in the discussion, we interpret Ivanščica belongs to the Pre-Karst zone of the Dinarides.\u003c/p\u003e \u003c/div\u003e"},{"header":"5. Conclusions","content":"\u003cp\u003e \u003cdiv class=\"BlockQuote\"\u003e \u003cp\u003eIvanščica Mt., an inselberg in the Alpine \u0026ndash; Dinaridic transitional zone of northern Croatia, is divided into three structural domains: Ivanščica Parautochton, Ivanščica Imbricates and Oligo-Neogene sedimentary cover.\u003c/p\u003e \u003cp\u003eBy implementation of a multi-scale structural analysis, AFT, and VR data, four contractional and one extensional event have been recorded on Ivanščica Mt. In addition, two older extensional events were recognized based on the Mesozoic tectono-sedimentary record. Middle Triassic (D1) and Early Jurassic (D2) extensional events related to the opening of the Neotethys Ocean and Alpine Tethys respectively are recorded in sedimentary successions of the SDIP and the SDII.\u003c/p\u003e \u003cp\u003eLate Berriasian to Valanginian (~\u0026thinsp;140 Ma) contraction (D3) is manifested with tectonic emplacement of the ophiolitic m\u0026eacute;lange of the Repno Complex over the stratigraphic successions of the Adriatic passive margin in the SDII and their thermal alteration.\u003c/p\u003e \u003cp\u003eFollowing contractional event (D4) manifested in NW-ward imbrication, thrusting of the SDII over the SDIP along the ČMT and thermal alteration of sedimentary succession of the SDIP. Syn-deformational Hauterivian to Albian Oštrc Fm. and our AFT modelling results provide age constraints for this deformational event (~\u0026thinsp;133\u0026ndash;100 Ma). When considering the post Oligo-Miocene rotations, initial NW trending and SW verging structures attributed to D4 deformational event coincide with the typical Dinaridic structural trend. This deformational event is a result of continued contraction related to the closure of the northern branch of the Neotethys Ocean and finally resulted in long lasting emersion in the Ivanščica Mt.\u003c/p\u003e \u003cp\u003eThe youngest extensional event (D5) is characterized by formation of NE-dipping predominantly listric normal faults and ENE striking dextral faults, as a consequence of ongoing extension in the Pannonian Basin. Timing of deformation is constrained by the Ottnangian to middle Badenian age (~\u0026thinsp;18\u0026ndash;14 Ma) of syn-rift deposits observed on the reflection seismic and well data. In the early post-rift stage, short lasting late Sarmatian contraction (~\u0026thinsp;12 Ma) is registered (D6), preceding the main stage of the basin inversion.\u003c/p\u003e \u003cp\u003eThe youngest recorded deformational event (D7) characterised by Late Pannonian (~\u0026thinsp;6 Ma) to recent NNW-SSE contraction, resulted in reactivation of ENE striking dextral faults, formation of new SE striking dextral faults as well as the formation of E to NE trending folds and reverse faults. This event is a result of N-ward indentation and CCW rotation of Adriatic microplate. Overall Miocene and post-Miocene deformational history of the study area is in align with well-known Pannonian back-arc tectonics starting in the Early Miocene.\u003c/p\u003e \u003cp\u003eOur results infer that the study area was affected by tectonic processes related to the different stages of the evolution of the Neotethys Ocean, opening of the Alpine Tethys Ocean, as well as the opening and inversion of the Pannonian Basin. Complete Mesozoic and Cenozoic tectono-sedimentary evolution of Ivanščica Mt. exhibits Dinaridic affiliation and allows its placement in the Pre-Karst zone of the Dinarides.\u003c/p\u003e \u003c/div\u003e \u003c/p\u003e"},{"header":"Abbreviations","content":"\u003cdiv class=\"DefinitionList\"\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eAFT\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eapatite fission track\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eAPAZ\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eapatite partial annealing zone\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eBZBT\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eBabin Zub back-thrust\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eCCW\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003ecounter clockwise\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eČMT\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eČrne Mlake thrust\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eDn\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003edeformational event (n is the number indicating the relative age of the event where the number 1 is the oldest event)\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eDLS\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eDinarides Lake System\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eGPF\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eGotalovec-Prigorec fault\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eMSWD\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003emean square of weighted deviates\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003en\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003enumber of used data\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eP(χ2)\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003eprobability of obtaining chi-square (χ2) for n degrees of freedom (n is the number of crystals\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eSDII\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003estructural domain Ivanščica imbricates\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eSDIP\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003estructural domain Ivanščica parautochton\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eSDONC\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003estructural domain Oligo-Neogene sedimentary cover\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eSSZ\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003esupra subduction zone\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv class=\"DefinitionListEntry\"\u003e \u003cdiv class=\"Term\"\u003eVR\u003c/div\u003e \u003cdiv class=\"Description\"\u003e \u003cp\u003evitrinite reflectance\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003c/div\u003e"},{"header":"Declarations","content":"\u003cp\u003e\u003cstrong\u003eAcknowledgements\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThe authors would like to thank to Matija \u0026Scaron;imunić for providing the photo in Fig. 5h.\u003c/p\u003e\n\u003cp\u003eThis research was supported by the Croatian Science Foundation under the project \u0026ldquo;Revealing the Middle Triassic Paleotethyan Geodynamics Recorded in the Volcano-Sedimentary Successions of NW Croatia\u0026rdquo; (IP-2019\u0026ndash;04-3824).\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eAuthor contribution\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eMatija Vukovski\u003c/strong\u003e:conceptualization, methodology, field work, analysis (structural), investigation, writing (original draft, review and editing); \u003cstrong\u003eMarko \u0026Scaron;pelić\u003c/strong\u003e: analysis (seismic sections), writing (original draft, review and editing); \u003cstrong\u003eDuje Kukoč\u003c/strong\u003e: field work, writing (original draft, review and editing); \u003cstrong\u003eTamara Troskot-Čorbić\u003c/strong\u003e: analysis (vitrinite reflectance), writing (original draft, review and editing); \u003cstrong\u003eTonći Grgasović\u003c/strong\u003e: field work, writing (review and editing); \u003cstrong\u003eDamir Slovenec\u003c/strong\u003e: writing (review and editing); \u003cstrong\u003eBruno Tomljenović\u003c/strong\u003e: conceptualization, methodology, field work, writing (original draft, review and editing)\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eFunding\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThis research was funded by the Croatian Science Foundation under the project \u0026ldquo;Revealing the Middle Triassic Paleotethyan Geodynamics Recorded in the Volcano-Sedimentary Successions of NW Croatia\u0026rdquo; (IP-2019\u0026ndash;04-3824).\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eData availability\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eAll data generated or analysed during this study are included in this article.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDeclaration of Competing Interest\u003c/strong\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eThe authors have no competing interests to declare that are relevant to the content of this article.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\u003cli\u003e\u003cspan\u003eAničić, B., \u0026amp; Juriša, M. 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Ivanščica (Northwestern Croatia). \u003cem\u003eActa Geologica\u003c/em\u003e, \u003cem\u003e11\u003c/em\u003e(1), 1\u0026ndash;44.\u003c/span\u003e\u003c/li\u003e\u003c/ol\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":false,"highlight":"","institution":"","isAcceptedByJournal":true,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"swiss-journal-of-geosciences","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"sjge","sideBox":"Learn more about [Swiss Journal of Geosciences](https://sjg.springeropen.com)","snPcode":"15","submissionUrl":"https://submission.nature.com/new-submission/15/3","title":"Swiss Journal of Geosciences","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"stoa","reportingPortfolio":"Springer Open","inReviewEnabled":true,"inReviewRevisionsEnabled":true},"keywords":"Northern Neotethys, Adriatic passive margin, ophiolite obduction, nappe stacking, imbricate fan, structural inheritance, tectonic inversion, Pre-Karst zone","lastPublishedDoi":"10.21203/rs.3.rs-3991799/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-3991799/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eA comprehensive study, including geological mapping, structural and thermochronological analysis, has been carried out on Ivanščica Mountain (NW Croatia), with the aim to contribute in reconstruction of the tectonic history of the Dinarides, Southern/Eastern Alps and Pannonian Basin transitional zone. Implementation of structural and thermochronological methods enabled a subdivision of Ivanščica Mt. into three structural domains (from bottom to top): Ivanščica Parautochton, Ivanščica Imbricates and Oligo-Neogene sedimentary cover. In addition, a sequence of deformational events in tectonic history of this transitional zone is proposed, comprising three extensional and four contractional events starting from Middle Triassic until present times.\u003c/p\u003e \u003cp\u003eOldest deformational events indicating Middle Triassic (D1) and Early Jurassic (D2) extensional phases were recognised only in volcano-sedimentary record. The oldest contractional event (D3) is related to obduction of the Neotethyan ophiolitic m\u0026eacute;lange over Upper Triassic to Lower Cretaceous succession of the eastern margin of the Adriatic microplate, which resulted in thermal alteration of the Ivanščica Imbricates structural domain in Berriasian - Valanginian times (~\u0026thinsp;140 Ma). This event was soon followed by another contractional event (D4), which resulted in thrusting and imbrication of the Adriatic passive margin successions together with tectonically emplaced ophiolitic m\u0026eacute;lange, thermal alteration of the footwall successions, fast exhumation and erosion. Apatite fission track data together with syn-tectonic deposits indicate Hauterivian to Albian age of this event (~\u0026thinsp;133\u0026ndash;100 Ma). These Mesozoic structures were rotated in post-Oligocene times and brought from initially typically Dinaridic SE striking and SW verging structures to recent SW striking and NW verging structures. Following extensional event (D5) manifested in the formation of SE striking and mostly NE dipping normal listric faults, and ENE striking dextral faults accommodating top-NE extension in the Pannonian Basin. Deformations were coupled with hanging wall sedimentation of Ottnangian to middle Badenian (~\u0026thinsp;18\u0026ndash;14 Ma) syn-rift deposit as observed from the reflection seismic and well data. Short lasting contraction (D6) was registered in the late Sarmatian (~\u0026thinsp;12 Ma). The youngest documented deformational event (D7) resulted in reactivation of ENE striking dextral faults, formation of SE striking dextral faults as well as the formation of E to NE trending folds and reverse faults. This event corresponds to Late Pannonian (~\u0026thinsp;6 Ma) to recent NNW-SSE contraction driven by the indentation and counterclockwise rotation of Adriatic microplate.\u003c/p\u003e \u003cp\u003eRecognized tectonic events and their timings indicate that Ivanščica was mainly affected by deformational phases related to the Mesozoic evolution of the Neotethys Ocean as well as Cenozoic opening and inversion of the Pannonian Basin. Mesozoic tectono-sedimentary evolution of Ivanščica Mountain exhibits clear Dinaridic affiliation, more precisely, that of the Pre-Karst zone of the Dinarides.\u003c/p\u003e","manuscriptTitle":"Unravelling the Tectonic Evolution of the Dinarides – Alps – Pannonian Basin Transition Zone: Insights from Structural Analysis and Low-Temperature Thermochronology from Ivanščica Mt., NW Croatia","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2024-02-29 04:32:07","doi":"10.21203/rs.3.rs-3991799/v1","editorialEvents":[{"type":"communityComments","content":0},{"type":"decision","content":"Revision requested","date":"2024-04-05T08:42:36+00:00","index":"","fulltext":""},{"type":"editorInvitedReview","content":"","date":"2024-03-07T11:10:20+00:00","index":"hide","fulltext":""},{"type":"reviewerAgreed","content":"1909e34f-7634-4f7f-be20-68239412dacb","date":"2024-03-02T09:43:50+00:00","index":"hide","fulltext":""},{"type":"reviewersInvited","content":"","date":"2024-03-01T13:51:10+00:00","index":"","fulltext":""},{"type":"checksComplete","content":"","date":"2024-02-27T12:32:54+00:00","index":"","fulltext":""},{"type":"editorAssigned","content":"","date":"2024-02-27T12:32:54+00:00","index":"","fulltext":""},{"type":"submitted","content":"Swiss Journal of Geosciences","date":"2024-02-26T19:22:45+00:00","index":"","fulltext":""}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"swiss-journal-of-geosciences","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"sjge","sideBox":"Learn more about [Swiss Journal of Geosciences](https://sjg.springeropen.com)","snPcode":"15","submissionUrl":"https://submission.nature.com/new-submission/15/3","title":"Swiss Journal of Geosciences","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"stoa","reportingPortfolio":"Springer Open","inReviewEnabled":true,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"7adaf6d3-b8c6-457f-9fbb-19d4806b0f29","owner":[],"postedDate":"February 29th, 2024","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"published-in-journal","subjectAreas":[],"tags":[],"updatedAt":"2024-09-09T16:18:10+00:00","versionOfRecord":{"articleIdentity":"rs-3991799","link":"https://doi.org/10.1186/s00015-024-00464-5","journal":{"identity":"swiss-journal-of-geosciences","isVorOnly":false,"title":"Swiss Journal of Geosciences"},"publishedOn":"2024-09-02 15:56:58","publishedOnDateReadable":"September 2nd, 2024"},"versionCreatedAt":"2024-02-29 04:32:07","video":"","vorDoi":"10.1186/s00015-024-00464-5","vorDoiUrl":"https://doi.org/10.1186/s00015-024-00464-5","workflowStages":[]},"version":"v1","identity":"rs-3991799","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-3991799","identity":"rs-3991799","version":["v1"]},"buildId":"qtupq5eGEP_6zYnWcrvyt","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}