Late Jurassic facies succession of the Kleszczów Graben area (southern border of the Łódź Depression, peri-Tethyan shelf, central Poland)

Abstract

Nu mer ous fully cored bore holes com pleted in the last years in cen tral Po land (Kleszczów Graben area, south ern bor der of the Łódź De pres sion) en abled the re search ers to ob tain new sedimentological data on the Oxfordian-Tithonian con tin u ous sed i men tary re cord in the Pol ish part of the north ern Tethys shelf. Twenty-two fa cies were dis tin guished in the sedimentological suc ces sion. The fa cies rep re sent the outer-, mid-and in ner-ramp en vi ron ments, in clud ing evaporitic ep isodes and palaeosols. The fa cies doc u ment that the Oxfordian-Lower Kimmeridgian (up to Hypselocyclum) car bon ate ramp has evolved to the Up per Kimmeridgian-Tithonian car bon ate-siliciclastic ramp. Among the Kimmeridgian de pos its, nu merous hardgrounds, tidal chan nel de pos its and grav ity flow sed i ments were iden ti fied. The Kleszczów Graben sed i men tary suc ces sion is dis cussed along with the lithostratigraphical units known from the ad ja cent re gions of south ern and cen tral Poland.

The oldest stage of the Outer Carpathian evolution in the light of Oxfordian–Kimmeridgian exotic clast studies (southern Poland)

“…The oncoid-intraclast-Crescentiella limestones (FT 2) dominated by various coated grains, bioclasts and intraclasts with numerous Crescentiella are commonly observed in many parts of Upper Jurassic, open marine, shallow-water platforms (above the storm wave base i.e., around 40-60 m depth) of the Tethyan Realm in the Central Europe (e.g., Leinfelder et al 1996;Krajewski and Olszewska 2006;Matyszkiewicz et al 2006Matyszkiewicz et al , 2012Schlagintweit and Gawlick 2008;Hoffmann et al 2017;Pleş et al 2017;Krajewski and Schlagintweit 2018; and references therein). On the northern Tethyan shelf area, such associations are common in a mid-ramp setting (e.g., Leinfelder et al 1996;Senowbari-Daryan et al 2008;Krajewski et al 2016Olchowy et al 2019). Both the oncoids and the aggregate coated Fig.…”

“…Usually, on the northern Tethys shelf, the Oxfordian-Kimmeridgian sponge-microbial limestones (FT 1) are interpreted as distal mid-ramp facies, i.e., deposited mostly in a low-energy, nutrient-rich environment. The FT 1 formed at estimated depths of some tens of meters, between the fairweather and the storm waves bases (e.g., Keupp et al 1993;Leinfelder et al 1996;Olóriz et al 2003;Olivier et al 2003;Reolid et al 2005;Matyszkiewicz et al 2006Matyszkiewicz et al , 2012Krajewski et al 2016Olchowy et al 2019).…”

Seismic Characteristics and Development of the Upper Jurassic Carbonate Buildups from the Miechów Trough (Southern Poland)

“…The central and southern Polish part of the Late Jurassic depositional system in the south was connected with the Tethys Ocean (e.g., [11,72,74,90]). The inner ramp facies, composed mainly of oolitic and oncolitic deposits and different bioclastic grainstones, formed the northward-, north-westwardand/or westward-prograding shallow-water carbonate platform (see e.g., [17][18][19]71,91]). The mid ramp facies represent mostly open shelf microbial-sponge deposits (e.g., [6,17,69,71,72,92]).…”

“…These diversified deposits, sometimes categorized under the general term "sponge megafacies" [93,94], are built of microbial structures (see e.g., [26,95]) and siliceous sponges, and are present within the northern Tethyan shelf in Europe [68,96,97]. The Oxfordian-lower Kimmeridgian carbonate ramp had evolved into a carbonate-siliciclastic ramp, represented by the upper Kimmeridgian-Tithonian facies ( [19]; cf., [16]). In general, during the Kimmeridgian and Tithonian, the lateral extent of this epicontinental basin was gradually decreasing [98,99].…”

“…The Upper Jurassic carbonate buildups of the northern Tethys shelf developed on extensive ramp-type platforms (e.g., [6,16,17]), and their differentiated deposits could be divided into three main compositional types: (1) coral-dominated, (2) siliceous sponge-dominated, and (3) microbialite-dominated (e.g., [3][4][5][6]8]). Intensive growth of the carbonate buildups took place mainly during the Oxfordian, sometimes up to the Kimmeridgian; in some basins, however, they might have developed locally even up to the Tithonian (e.g., [4,6,8,[18][19][20][21][22]). The microbial crusts (see e.g., [23][24][25] for more details concerning microbial structures) play important roles not only within the microbial facies, but also in the sponge and coral facies, where they occur in variable quantities ( [1]; see also [26,27]).…”