Marton.indd 107 �Geologia CroaticaGeologia Croatica AB STRA CT For the purpose of this work samples for palaeomagnetic analysis were taken from Upper Cenomanian and Lower Senonian shallow water limestones, as well as from Senonian pelagic limestones from both Ist and the surrounding islands. This area belongs to Imbricated Adria, which is characterized by gently folded and faulted strata with a Dinaridic (NW–SE) trend. An exception is Premuda island where the beds are strongly folded and are subvertical. A total of 96 samples were drilled from 10 localities distributed between eight islands. The samples were then sub- jected to standard palaeomagnetic laboratory analysis and statistical evaluation. Eventually, six localities yielded sta- tistically well-defi ned palaeomagnetic directions, which were shown pre date the folding in age. The overall mean palaeomagnetic direction obtained for the study area, characterizing the Cenomanian–Early Seno- nian time period had a Declination of 334°, Inclination=+46°, with statistical parameters k=188, a95=4.9°, defi ning a palaeomagnetic pole at l(N)=63°, f(E)=254°, dp=4.0°, dm=6.2°. This was compared with palaeomagnetic direc- tions obtained for rocks of similar ages from stable Istria and the Kvarner islands. As the three palaeomagnetic direc- tions are statistically identical, we conclude that there was no signifi cant relative movement between the three areas after the Early Senonian. The palaeomagnetic declination for the study area, which characterizes the post-Early Senonian rotation of the Adria- tic microplate, is the same as the declination for the Pannonian–Pontian age group from the South Pannonian basin. As the palaeomagnetic signals in both cases are primary, the results of the present paper not only support the conclu- sion that the rotating Adriatic microplate triggered rotations in the South Pannonian basin, but also suggest that the Adriatic platform did not change its orientation between the late Cretaceous and the Early Pontian. Keywords: imbricated Adria, palaeomagnetism, Late Cretaceous New palaeomagnetic results from imbricated Adria: Ist island and related areas � Emő Márton1 and Alan Moro2 1 Palaeomagnetic Laboratory, Eötvös Loránd Geophysical Institute of Hungary, Columbus 17–23, 1145 Budapest, Hungary; (paleo@elgi.hu) 2 Department of Geology, Faculty of Science, University of Zagreb, Horvatovac 102A, 10000 Zagreb, Croatia; (amoro@geol.pmf.hr) doi: 10.4154/gc.2009.09 Geologia Croatica 62/2 107–114 10 Figs. 2 Tabs. Zagreb 2009 1. INTRODUCTION Tectonically oriented palaeomagnetic studies in Croatian ter- ritory started in the 1980s. The fi rst results were published from Cretaceous rocks of stable Istria (area 1 in Fig.1, MÁRTON & VELJOVIĆ, 1983), followed by a number of papers concern- ing imbricated Istria and the Kvarner islands (MÁRTON & VELJOVIĆ, 1987, Fig. 1, areas 2–3), Kvarner islands (MÁR- TON et al., 1990) and Dugi Otok (Fig 1., area 4) and Vis (Fig. 1, area 5) Islands (MÁRTON & MILICEVIĆ, 1994). These results were obtained on platform carbonates which contain extremely small amounts of magnetic minerals, the- refore, their bulk susceptibilities are invariably diamagnetic and their natural remanent magnetizations are of very low intensities. Consequently, platform carbonate samples some- times fail to yield palaeomagnetic signals. Sometimes the palaeomagnetic directions have poor statistical parameters, as has been shown in pioneering work on the Adriatic plat- form carbonates. Nevertheless, there are quite a number of Geologia Croatica Geologia Croatica 62/2 108 Fi gu re 1: Sketch map of Croatia with main thrust fronts (after TARI, 2002 and MIKES et al., 2008). The areas of previous palaeo- magnetic investigations are shaded. 1 – Stable Istria (MÁRTON & VELJOVIĆ, 1983, MÁRTON et al., 2003, 2008), 2 – Imbricated Istria and Kvarner islands (MÁRTON & VELJOVIĆ, 1987), 3 – Kvarner islands (MÁRTON et al., 1990), 4,5 – Dugi Otok and Vis (MÁRTON & MILICEVIĆ, 1994), 6,7,8 – Medvednica Mt., Ivancica Mt., Poz- eska Mt, Krndija Mt. and Papuk Mt. (MÁR- TON et al., 1999, 2002, 2005), 9 – Krsko and Karlovac basin (MÁRTON et al., 2006). Fi gu re 2: Simplifi ed geological map (after MAMUZIĆ, 1970 and MAMUZIĆ et al. 1970), with the palaeomagnetic sampling locali- ties 1–10. Geologia CroaticaEmő Márton and Alan Moro: New palaeomagnetic results from imbricated Adria: Ist island and related areas 109 previously published palaeomagnetic directions which have passed the present strict criteria developed to ensure good- quality data (see. MÁRTON et al., 2008) Intensive and systematic palaeomagnetic investigation started in the early 1990s in two areas. The study of Adriatic platform carbonates (Fig. 1, area 1) resulted in the defi nition of an apparent polar wander path (APW) for the Tithonian through mid-late Eocene periods of time for stable Istria (MÁRTON et al., 2003, 2008). In the South Pannonian basin (Fig. 1, area 6–9), the targets were Tertiary rocks, which show ed counter-clockwise (CCW) rotations of post-Early Pontian age. These rotations were interpreted as having been trig- gered by the CCW rotating Adriatic microplate (MÁRTON et al., 1999, 2002, 2005). Palaeomagnetic observations in the area between the southern Pannonian basin and stable Istria are poorly distri- buted. As these observations are mostly from the 1980s, obser- vations since 2006 have been concentrated on the tectonically more complicated External Dinarides. The present paper is an initial step in this vein, as it deals with the palaeomagnet- ism of an area belonging to the imbricated margin of stable Adria. 2. GEOLOGICAL BACKGROUND Ist Island and its surrounding islands (Fig. 2), which are pa- laeogeographically part of Adriatic carbonate platform (VLA- HO VIĆ et al., 2005), belong to a geotectonic unit, known variously as Adriaticum (HERAK, 1991), or Imbricated Adria (TARI, 2002) depending on the geotectonic interpretation. The region is characterized by gently folded and faulted Cre- ta ceous and Palaeogene strata (which transgressively overlie the Cretaceous, MAMUŽIĆ & SOKAČ, 1967; MORO & JELASKA, 1994; ĆOSOVIĆ et al., 1994), with a Dinaridic (NW–SE) trend. An exception is Premuda island where the beds are strongly folded. Our study area is situated (Fig. 1) practically halfway between stable Adria and the Western thrust belt (TARI, 2002) or Dinaricum (HERAK, 1991). In the study area, Upper Cretaceous, shallow water, per- itidal limestones prevail (VLAHOVIĆ et al., 2005), which range in age from the Cenomanian–Lower Senonian (MA- MUŽIĆ & SOKAČ, 1967; MORO & JELASKA, 1994). Early Turonian pelagic sediments deposited on a drowned platform are the exception (GUŠIĆ & JELASKA, 1990; MORO et al., 2002; VLAHOVIĆ et al., 2005). During the Mid Turonian, shallow-water sedimentation was re-established on Olib Is- land, while at Silba, Premuda and Ist islands pelagic sedimen- tation continued until the Senonian (KAPOVIĆ & BAUER, 1970; MORO, 1993). On most islands, strata are subhorizontal (Fig. 3) or SW and NE dipping with angles up 25° (Fig. 2). An exception is Premuda island with subvertical beds (Fig. 4). Shallow water peritidal limestones are characterized by the vertical alteration of intertidal laminites and subtidal lime- stones. Subtidal limestones appear in two varieties: foramini- feral wackestone-packstones, rarely grainstones and rudist or chondrodonta fl oatstones. Depositional environments of these limestones were the shallow and protected parts of the carbon- ate platform. The pelagic limestones are characterized by the massive pelagic limestones with lenses of resedimented shal- low water material, which could be in alteration with lami- nated pelagic limestones. The depositional environment could be deterrmined as a transition between the shallow platform and deeper basin (KAPOVIĆ & BAUER, 1970). 3. PALAEOMAGNETIC SAMPLING For the purpose of this work, samples were taken from Up- per Cenomanian and Lower Senonian shallow water lime- stones, as well as from Senonian pelagic limestones for pa- laeomagnetic studies. The strata sampled were invariably light grey or white in colour. Samples were drilled and ori- ented in the fi eld with a magnetic compass. Beds with shal- low dips were preferred, though at one locality (Premuda) subvertical strata were sampled (Fig. 4). Tilts of the sampled strata were recorded and used later, during the evaluation of the data as correction parameters for restoring the horizontal position of the beds. Fi gu re 3: Subhorizontal beds at Ist is- land (locality 5) with palaeomagnetic boreholes (arrow). Geologia Croatica Geologia Croatica 62/2 110 The sampling localities are distributed over several is- lands, partly because of the character of the region, partly because several outcrops on the larger islands were heavily karstifi ed (e.g. Olib, Silba). Among the sampling localities there are abandoned quarries (localities 5, 6 and 8 on Fig. 2) as well as natural coastal outcrops. Eventually, 96 samples were collected from 10 geographically distributed localities (Fig. 2 and Table 1). 4. LABORATORY PROCESSING AND RESULTS The samples were cut into standard-size specimens and the natural remanent magnetization (NRM) as well as the mag- netic susceptibility of each specimen was measured in the laboratory. The instruments used were JR4 and JR5A mag- netometers and a KLY-2 Kappabridge. In case of magnetic intensities exceeding 12x10–5 A/m, one of the specimens (if the core was long enough to provide sister specimens) were demagnetized stepwise using the alternating fi eld (AF) meth od, the other using the thermal method. At lower NRM intensi- ties, both specimens were demagnetized with AF, (as years of experience with extremely weakly magnetic platform car- bonates from Istria showed that the thermal method was not practicable in such cases, MÁRTON et al., 2003, 2008), and the better defi ned demagnetization curve of the sister speci- mens was used for evaluation. The fi rst step of the evalua- tion was component analysis (KIRSCHVINK, 1980) of the Table 1: Locality mean palaeomagnetic directions with statistical parameters for Ist island and related areas. Key: n/no: number used/collected sam- ples (the samples are independently oriented cores), D, I, DC, IC: Declination, Inclination before and after tilt correction, k and a95: Statistical parameters (FISHER, 1953). Locality Lat. Long. N/No Do Io k α95 o DC o IC o k α95 o dip 1 Ist, port HR 953-961 44°16’44.8” 14°45’25.5” 7/9 340 +52 21 13 329 +42 42 9 314/10 252/25 2 Silba, Nozdre bay HR 962-971 44°21’19.7” 14°43’24.3” 6/10 328 +40 55 9 334 +48 55 9 110/10 3 Olib, Sv. Nikola port Hr 972-80 44°21’19.9” 14°46’23.1” 0/9 too weak 4 Škarda Hr 981-86 44°16’23.7” 14°42’58.6” 0/6 too weak 5 Ist, abandoned quarry HR 987-995 44°15’22.9” 14°45’54.6” 9/9 336 +49 108 5 338 +48 108 5 42/2 6 Tramerka HR 996-904 44°13’21.9” 14°46’08.0” 6/9 337 +51 230 4 325 +45 230 4 271/12 7 Premuda, Široka bay HR 1137-154 44°19’05.3” 14°37’52.5” 5/18 3 –20 73 9 347 +45 73 9 219/82 8 Funestrala HR 1155-166 44°15’07.9” 14°44’39.0” 8/12 330 +44 98 6 332 +48 98 6 125/5 9 Molat, Vodomarka bay, HR 1167-172 44°14’17.1” 14°15’21.0” 6/6 great circle distribution 10 Ist, Kosirača bay HR 1173-80 44°17’5.5” 14°45’21.5” 0/8 too weak Fi gu re 4: Subvertical beds at Premuda island (locality 7) with palaeomagnetic boreholes (arrow). Geologia CroaticaEmő Márton and Alan Moro: New palaeomagnetic results from imbricated Adria: Ist island and related areas 111 demagnetization plots for linear segments. As Figs. 5 and 6 show, the demagnetization curves sometimes exhibit a single component, going practically to the origin (Fig. 5, specimen HR 991). However, the NRM is often composite, (despite the fact that the only magnetic mineral in the collected sam- ples is magnetite, as Fig. 7 suggests), especially that of sam- ples with stronger palaeomagnetic signals, (the demagneti- zation curves in Figs. 5 and 6, except HR 991). In all cases, the components ending at or close to the origin were chosen to represent the characteristic remanence (ChRM) of a sam- ple, and the locality mean palaeomagnetic directions were calculated from one direction per independently oriented sample. As Table 1 documents, all locality mean palaeomag- netic directions have good statistical parameters and depart signifi cantly from the present north. Thus, they can be con- sidered as well-defi ned palaeomagnetic signals and as syn- Fi gu re 5: Typical demagnetization curves. AF demagnetized specimens from locality 5 showing the varied NRM intensities and the behaviour of the NRMs on demagnetization. Zijderveld diagrams plus normalized NRM intensity versus AF fi eld. Key to the Zijderveld diagrams: fi lled circles are the pro- jection of the palaeomagnetic vector onto the horizontal plane; open circles, projections onto the vertical plane. Fi gu re 6: Typical demagnetization curves. AF demagnetized specimens from locality 8 (HR 1156 and HR 1162), documenting that after the removal of the overprint component, which is of diff erent directions for the two specimens, the ChRMs are of similar directions. An AF demagnetized specimen from locality 6 (HR 996) and a thermally demagnetized one from locality 7 (HR 1144). Key is as for Fig.5, but for the last sample the smaller diagram is an inten- sity (circles) / susceptibility (dots) versus temperature diagram. Geologia Croatica Geologia Croatica 62/2 112 folding Fisher analysis shows, they predate the age of folding (Table 2 and Fig. 8). The ChRMs of one locality (Vodo - marka) were not suited for evaluation by the Fisher method since they exhibit a great circle distribution. This great circle (in the tectonic system) closely passes by the group of tilt- corrected palaeomagnetic directions of the other localities, suggesting that the component of the pre-folding age is simi- lar to the ancient magnetic directions of other localities (Fig. 9). However, the statistical parameters for the overall palaeo- magnetic direction are better without the locality of Vodomarka. Therefore the Cenomanian–Early Senonian of the study area is based on six geographically distributed localities (Table 2). 5. DISCUSSION AND CONCLUSIONS The overall-mean palaeomagnetic direction predating the age of folding for the study area characterizes the Cenoma- nian–Lower Senonian time period. Palaeomagnetic direc- Fi gu re 8: Locality mean palaeomagnetic directions with confi dence circles before (left stereogram), and after (right stereogram), tilt corrections. The mid- dle diagram shows the result of the syn-tilting Fisher analysis. The best grouping of the locality mean palaeomagnetic directions is achieved close to 100% unfolding and the peak is extremely high, meaning that the test is signifi cant. Table 2: Oveall mean palaeomagnetic directions for Cenomanian–Early Senonian localities, before and after tilt corrections with statistical parameters and palaeomagnetic poles calculated from the tilt-corrected directions for Ist island and related areas, for stable Istria (the fi rst version comprises the Cenomanian and Early Senonian localities, the second also Turonian localities) and for the Kvarner islands. N D° I° k α95° DC° IC° k α95° l(N) f(E) δp δm Study area Cenomanian+lower Senonian 6 340 38 8 25.4 334 46 188 4.9 63 254 4.0 6.2 Stable Istria Cenomanian+Coniacian 8 323 45 44 8.5 334 51 65 7.5 66 259 6.9 10.1 Cenomanian–Coniacian 12 325 44 54 5.9 334 50 60 5.7 65 257 5.1 7.6 Kvarner islands Cenomanian–Turonian 6 309 45 33 11.9 327 47 27 13.1 59 263 10.9 16.9 Fi gu re 7: Magnetic mineralogy experiments. The acquisition behaviour of the isothermal remanent magnetization indicates magnetite as the only magnetic mineral in the samples. Geologia CroaticaEmő Márton and Alan Moro: New palaeomagnetic results from imbricated Adria: Ist island and related areas 113 tions published for rocks of similar ages are known from stable Istria and the Kvarner islands, the fi rst representing the hard core of the Adriatic microplate (MÁRTON et al., 2003, 2008), the second the NW part of imbricated Adria. Before such a comparison it has to be emphasized that the results for the Cenomanian–Early Senonian time period of the present study are superior to those previously obtained from stable Istria and the Kvarner islands, in the sense that the age of the magnetization is better constrained. This is because the syn-tilting Fisher analysis yields the best statis- tics close to 100 % unfolding for the study area (Table 2) and the statistical improvement is signifi cant (Fig. 8), while in the previously published cases the age of the magnetizations are not so tightly connected to the age of the sampled rocks. Nevertheless, the overall-mean palaeomagnetic directions for the Cenomanian–Early Senonian time period for the three above mentioned areas (Fig. 2) have statistically iden- tical overall palaeomagnetic directions (Fig. 10). This situ- ation has an important tectonic implication, which is the lack of large scale relative movement between the respective areas, after the Early Senonian. In other words, stable Istria and at least the NW part of its imbricated margin can be treated as a rigid block in the course of plate tectonic dis- placements from the late Cretaceous onwards. The declination of the overall-mean palaeomagnetic di- rection obtained for the study area is 334°. Interestingly, the palaeomagnetic declination for a combined Pannonian–Pon- tian group of localities for the Southern Pannonian basin is also 334° (MÁRTON et al., 2002). As the palaeomagnetic signals in both cases are primary, the results of the present paper not only support the conclusion that the rotating Adri- atic microplate triggered rotations in the South Pannonian basin (MÁRTON et al., 2002, MÁRTON, 2006), but also suggest that the Adriatic platform did not change its orienta- tion between the late Cretaceous and the Early Pontian. 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Res., 23, 489–508. doi: 10.1006cres.2002. 1017 TARI, V. (2002): Evolution of the northern and western Dinarides: a tectonostratigraphic approach.– EGS Stephan Mueller Publication Series, European Geophysical Society, 1, 1–21. VLAHOVIĆ, I., TIŠLJAR, J., VELIĆ, I. & MATIČEC, D. (2005): Evo- lution of the Adriatic Carbonate Platform: Palaeogeography, main events and depositional dynamics.– Palaeogeogr., Palaeoclimatol., Palaeoecol., 220, 333–360. doi: 10.1016/j.palaeo.2005.01.011 Manuscript received November 21, 2008 Revised manuscript accepted May 14, 2009 Available online June 19, 2009