An overview on Structural position of Mesozoic succession of distal Adriatic continental margin on Ivan&#353;&#269;ica Mt. (NW Croatia)
Authors: Vukovski Matija , Kukoč Duje , Tomljenović Bruno 
Published: March 2021

&lt;p&gt;Mt. Ivan&amp;#353;&amp;#269;ica is one of inselbergs in the Internal Dinarides (NW Croatia) in the transitional area with Southern Alps. In this area, NNW-verging Dinaric structures are overprinted by S-verging Alpine structures. Mt. Ivan&amp;#353;&amp;#269;ica is composed of Mesozoic shallow to deep-marine sedimentary succession of the passive continental margin of Adriatic plate, which was facing the Neotethys ocean, overthrust by ophiolitic m&amp;#233;lange. Here, we aim to present new preliminary structural data from pelagic sediments of Ivan&amp;#353;&amp;#269;ica Mt. in attempt to better understand tectonic history of this part of Internal Dinarides.&lt;/p&gt;&lt;p&gt;Mesozoic succession of Mt. Ivan&amp;#353;&amp;#269;ica is composed of Triassic clastic, volcanic and carbonate rocks overlain by Upper Triassic to Lower Jurassic shallow-marine carbonates. These are overlain by Jurassic pelagic carbonates and cherts followed by Tithonian&amp;#8722;Valanginian pelagic &amp;#8220;Aptychus Limestones&amp;#8221;. The uppermost part of this succession is composed of Lower Cretaceous O&amp;#353;trc fm., which conformably overlies the &amp;#8220;Aptychus Limestone&amp;#8221;. The O&amp;#353;trc fm. is characterized by turbidites with ophiolitic detritus and represents syn-orogenic deposits presumed as formed in a front of advancing ophiolitic nappe(s).&lt;/p&gt;&lt;p&gt;The focus of our investigation is primarily on structural characteristics of the &amp;#8220;Aptichus Limestones&amp;#8221; and the O&amp;#353;trc fm. The character of the contact between the &amp;#8220;Aptychus Limestones&amp;#8221; and underlying Upper Triassic to Lower Jurassic carbonates is still uncertain. According to &amp;#352;imuni&amp;#263; et al. (1982) &amp;#8220;Aptychus limestones&amp;#8221; unconformably overlays Triassic carbonates in periclinal geometry, while Babi&amp;#263; (1974) suggests continuous condensed pelagic sedimentation throughout the Jurassic. In contrast with previous observations and interpretations, our observations suggest a tectonic contact, characterized by significantly different orientation of bedding and locally marked by fault gauge (clay) seams.&lt;/p&gt;&lt;p&gt;Structural analysis shows numerous gentle to open asymmetric folds in the &amp;#8220;Aptychus Limestones&amp;#8221; and closed chevron folds and isoclinal folds in overlaying O&amp;#353;trc fm. Chevron folds and open to gentle asymmetric folds indicate NW vergence in present day orientation with fold axis parallel to the strike of the contact with underlying unit. Although different in shape and size, these folds are likely formed during the same tectonic event while their geometry is controlled by differences in rheological properties. Isoclinal folds occurring exclusively at the contact with ophiolitic m&amp;#233;lange are characterized by E-W oriented fold axis and S dipping axial surfaces which is in a contrast with aforementioned folds. Thus, we assume that these folds originated from another, presumably older tectonic event. Bedding in Triassic dolomites uniformly dips towards the SE. Local occurrence of condensed pelagic limestones and radiolarian cherts is interpreted, as rheologically weak horizon ideal to form a d&amp;#233;collement that, at least locally, could be interpreted to mark a thrust fault.&lt;/p&gt;&lt;p&gt;Formation of isoclinal folds in the O&amp;#353;trc fm. and the tectonic contact with ophiolitic m&amp;#233;lange is preliminarily attributed to the Aptian-Albian nappe stacking known from the Internal Dinarides. In addition, we assume that the pelagic succession of the &amp;#8220;Aptychus Limestones&amp;#8221; together with the overlying O&amp;#353;trc fm. and the ophiolitic m&amp;#233;lange are thrusted over the Upper Triassic to Liassic carbonates sometime later, possibly during the final stage of Neotethys closure in the Internal Dinarides.&lt;/p&gt;