The Pannonian Basin is a continental back-arc basin. Palaeomagnetics defined three terranes: Alcapa (Alps–Carapathians–Pannonian), Tisza–Dacia and Dinarides, rotated counterclockwise, clockwise and counterclockwise, respectively, in the Early and Middle Miocene. The timings and the extent of rotations suggest the terranes experienced differential internal rotations. Metamorphic core complexes occur along the margins and an internal part of the Pannonian Basin. Metamorphic core complexes display extension parallel then perpendicular to the margins. Low-temperature thermochronology defined that synrift exhumation occurred c. 18–16 Ma, coeval with map-view rotations. Microtectonic measurements evidenced superimposed fault patterns. When combined with palaeomagnetics, these patterns simplify to north–south compression throughout Late Paleogene–Middle Miocene. Complications result from rotating blocks deforming under this external stress field. Interpretation of seismic reflection data suggest that synrift phase was characterized by two perpendicular extensions. When rotations are considered, these resolve in east–west stretching. Strike-slip faulting during the Late Miocene accommodated differential movement of terranes pulled eastwards by slab roll-back along the Carpathians. Several inversions affect Late Miocene–Recent sediments. These are most intense and earliest in the SW Pannonian Basin, but also propagate into the internal parts. Rotational indentation of Adria into the Southern Alps–Western Dinarides is the main cause for inversion. Neotectonics reflect this inversion, that is enhanced by eastwards escaping Eastern Alps.

Analysis of seismic sections and wells near the frontal folds of Iraqi Kurdistan (Low-and Highly folded zone) document the interplay of folds, faults and possible mechanisms of their generation.Serial sections from 3D seismic volume in the Low folded zone are interpreted based on calibration wells. Sections display fold evolution from low amplitude kinked monocline to high amplitude ramp folding. The fold continues towards the exposed Safeen anticline with a subvertical limb. These lowland sections can also be considered as the lateral growth segment of Safeen anticline.Three geoseismic sections through frontal folds were constructed with variable quality seismic and dips, formation tops from surface and from mountains wells. These sections show tight anticlines with thrust faults cutting to near surface on both limbs; remnant normal faults; a subvertical southern limb crossed by flat thrusts; and a Triassic ductile core.Sections suggest that this part of Zagros is built of two 'rigid' units: an upper, Mesozoic-Neogene and a lower, Paleozoic one, separated by a ductile detachment along the lower Triassic. The upper unit is prone to folding and faulting, the lower one to faulting. The detachment in-between comprises the Kurrachine C, lower Triassic Beduh and Mirga Mir formations, and potentially the top members of Permian Chia Zairi formation. Detachment is possibly dominated by evaporites. Our detachment is thicker than only Beduh-Mirga Mir detachment proposed by recent reconstructions of others.Folds are initiated as detachment folds above thickened parts of the Lower Triassic, then evolve into ramp folds. Ramp is formed by the merger of flat thrusts with pre-existing steep earlier normal faults that affect the Mesozoic section. Shear and drag beneath these ramps lead to steepening of the southern limb and to fault propagation. A basal flat thrust is the final element of this fault propagation stage. Underlying rigid Paleozoic can form imbricates that push the Triassic detachment upwards, creating passive folds. These Paleozoic imbricates dip to the south and not to the north, as suggested by reconstructions of others. Finally, strike slip shear documented at outcrops also contributes to the final fold form.Own and others' surface geological observations, indications from seismic and radiometric data suggest that fold generation started in Late Cretaceous, continued in the Paleogene in internal Highly folded zone. In our study area only Late Neogene fold growth can be documented, which is in harmony with 5-8 Ma uplift dates of others. Others' geomorphologic work suggests fold lateral growth is a quick process. We propose that regional folds, such as Safeen anticline grow in distinct short periods separated by longer quiet intervals.

In Kurdistan Region of Iraq, the southern front of the Zagros fold belt is expressed by a series of folds trending NW-SE and E-W. Previously the existence of a main frontal thrust was suggested based on sharp topographic breaks along the frontal anticlines. Field mapping, structural analysis of seismic sections and wells revealed that these fold trains are affected by conjugate reverse faulting. Some minor portions of this thrusting can be mapped on the surface, sometimes combined with left-lateral strike slip movement. These thrusts link several detachments, some of which can be observed also on the surface. No expressed main boundary thrust was found, but such structures might be present at deep detachment level.

A fracture study was performed in Kurdistan Region of Northern Iraq. Based on exploration efforts, the Sargelu and Kurrachine carbonates are fractured reservoir rocks in the region. The study was based on traditional fieldwork. Data were collected in 6 anticlines and 9 formations. Orientation data of all fractures, faults within several blocks of 1 square metre were recorded, together with their length, aperture, frequency, filling, surface characteristics. Data were plotted on stereonets in present state, and in back-tilted (unfolded) state. Analysis was performed in latter position. Data were separated into layer-perpendicular and layer-oblique sets. Part of the fracture sets shows clear relation to local folding. Perpendicular (tensional) and shear joints form symmetrical sets. In these cases there are two oblique/shear sets: one where the acute angle bissectix points to the shortening direction and another, which has the obtuse angle bissectix in the same direction. In some other fracture sets there is strong departure from the local fold orientation. In these cases the different fracture sets can be interpreted as born of the superposition of two symmetric sets related to different fold orientations. This is supported by the measurement of NW-SE to E-W fold axes in the mentioned folds and areas, irrespective of the map attitude of the major folds. Layer-oblique sets were separated into three classes. Steeply dipping joints that were striking parallel to layer-perpendicular family of the same exposure were affiliated to fold-related joints. Flat-dipping fractures were possibly formed by compression. These fractures suggest compression directions. Finally, fractures having dips around 50° were interpreted as normal fault-like shear surfaces. These fractures suggest extension directions. Assessing the estimated structural directions we propose three probable extension events in N-S (NNW-SSE); NE-SW and NW-SE direction. The same exercise suggests (much weaker defined) NW-SE; NE-SW and N-S compression directions. Fault slip measurements in the closer and wider vicinity gave the same or very similar faulting events. In some exposures non-gravitational open fractures and others filled by bitumen were observed. These were mostly longitudinal joints, oriented perpendicular to recent local N-S or NE-SW compression, or shear joints symmetrical to these directions. Longitudinal joints may have remained open due to continuous fold growth. Shear joints may have remained open due to fold-parallel extension, or continuous shear movement. Since recent compressive stress directions play an important role in opening fractures (that are then filled by bitumen), oil migration should be a young process.

The Pénestin section (southern Brittany) presents large regular undulations, commonly interpreted as evidence of periglacial pingos. It is an upper Neogene palaeoestuary of the Vilaine River reactivated during the middle Quaternary (middle terrace). It is incised into a thick kaolinitic saprolite and deformed by saprolite diapirs. This paper presents the arguments leading to a mechanistic interpretation of the deformations at Pénestin. Neither recent transpressive tectonics nor diagnostic evidence of periglacial pingo have been found despite evidence for a late paleo-permafrost. The major deformational process is shale diapirism, initially triggered by co-seismic water supply, with further loading and lateral spreading on an already deformed and deeply weathered basement, which allowed the shale diapirism to develop. Deformations are favoured by the liquefaction of the saprolite and a seaward mass movement and recorded, rather distant, effects of an earthquake (c. 280 ka B.P.) resulting from the progressive subsidence of the southern Armorican margin. These deformations triggered by an earthquake are similar to those induced by classical shale diapirism. They are probably common in tectonically active continental environments with shallow water table.

The studied area is located in the Kohat Plateau in NW Pakistan in a collision zone resulted by N-S convergence of Eurasia and India. It was less explored area until 1999, when the MOL Plc. with Pakistani partners started a hydrocarbon exploration program. A detailed structural analysis was carried out on the basis of integrated interpretation of field, seismic and borehole data. All seismic data (2D, 3D, old and new) were jointly interpreted, seismic attribute analysis and balancing study were also applied. Two different structural levels can be identified which are composed of different formations. Both of them have own detachment surfaces. Two different tectonic regimes created the complexity of the region, older thin skinned fault bend folds and younger wrench tectonics. The same shortening can be found in the structural maps of horizons of different ages, thus presumably the same stress field formed the different tectonic levels. The most characteristic structures are the thrust faults with southward vergence, but eastwards this trend is flexed towards ENE. Secondary en echelon folds with ENE-WSW axial direction are superposed to the general E-W directed structures. Significant oil and gas fields were discovered in several antiforms by the exploration program.

Paleomagnetic analyses were carried out on samples from 19 localities within two different mega-tectonic units in Northern Romania: Tisza-Dacia (11 localities) and ALCAPA (8 localities). The samples cover a range of different lithologies: (1) Late Cretaceous red-coloured marl to marly limestone, (2) EoOligocene flysch sediments, and (3) mid-Miocene (Langhian) tuffite (Dej tuff and related sediments). The Late Cretaceous and mid-Miocene specimens carry secondary paleomagnetic signals exhibiting a counter clockwise deflection of the paleo-declinations by some 30°, while the Eo-Oligocene localities indicate an overall clockwise deflected (between some 45° and >90°) paleodeclination with respect to present-day north. Clockwise rotation postdates the age of sedimentation (Lower Oligocene), as well as (at least partially) thrusting of the Pienides onto the Tisza-Dacia mega-tectonic unit, which occurred between 20.5 and 18.5 Ma. Clockwise rotation predates post-12 Ma counter clockwise rotations inferred for the mid-Miocene localities. Surprisingly, the clockwise rotations of the first rotational stage not only affected the (par-) autochthonous sedimentary cover of the Tisza-Dacia megatectonic unit, but also the allochthonous flysch nappes of the Pienides, i.e. the eastern tip of the ALCAPA mega-tectonic unit. Well-documented opposed rotation of the remainder of ALCAPA necessitates a detachment of this eastern tip of ALCAPA after 18.5 Ma. The most likely location for this detachment zone is along the margins of the Transcarpathian depression. During a second (post-12 Ma) stage, counter clockwise rotations of up to 30° affected the entire working area. Regarding timing and magnitude, these second stage rotations are similar to rotations documented for the East Slovak basin, but different from those reported from the South Apuseni Mountains and the Central and Inner West Carpathians located west of the East Slovak basin. ZUSAMMENFASSUNG

The Upper Aptian to Lower Albian Tata Limestone Formation consisting of brown-grey bioclastic crinoidal limestone presumably represents the first unconformable formation, which recorded early deformation events of the Alpine cycle. The base of the Tata Limestone is affected by erosional features accompanied by significant breccia bodies. Reconstruction of the paleomorphology of the basin bottom supported by paleoecological (e.g. water depth) data shows (in the recent orientation) at least five northwest-southeast trending zones with significant erosional features and accompanied by coarse-grained graded breccia in a more clayey matrix (e.g. Cseh-1 borehole). These elevations were uplifted above deeper basins filled with crinoidal limestone. The geometry of the uplifted units is asymmetrical, anticline-like and the deeper depressions have a syncline-like structure. According to previous works to the anticline-like morphology of the uplifted zones and to the transport direction of the coarse breccia clasts, these uplifted units were possibly formed by thrusting, in a compressional regime. The differences in the thickness of the crinoidal limestone and the breccia interbeds show synsedimentary character Of these Movements. In the borehole Cseh-1, large limestone fragments appear already in the Sumeg Marl Formation and they are present throughout all the Tata Limestone sequence. This fact indicates that the tectonic movements started in the Barremian and continued during the whole Aptian.

Quaternary and directly underlying Late Miocene (Pannonian) outcrops were analysed by structural, tectono-morphologic and sedimentologic methods to describe the main fault directions, to separate mass movements from faulting and folding and to separate earthquake-induced sediment deformations from other (e.g. periglacial) effects in the Somogy Hills. This is a gentle hilly area elevated at 200-300 m above sea level, located immediately south of Lake Balaton, Hungary.Quaternary outcrops showed several consistent directions of faulting, and co-depositional seismic activity. Three different Mohr-sets of faults/joints could be differentiated in Quaternary sediments. The three sets are considered Late Quaternary since all cut young loess sections and have morphological expressions. On the basis of the microtectonic measurements and morphotectonic investigations, the following sequence of Quaternary events can be proposed:1. A (W)NW-(E)SE compression and perpendicular extension would create E-W to WNW-ESE oriented right lateral, NNW-SSE to N-S oriented left lateral shear zones, and NW-SE striking normal faults. Some of these can be evidenced in morphology and among the individual fault measurements. Some reactivated faults might suggest that this field is a relatively older one, but fresh topographic elements suggest that this stress field might be operational sub-recently.2. A second stress field with NNW-SSE extensional and ENE-WSW oriented compressional directions could be separated. This stress field could create NNE-SSW and NW-SE oriented shear fractures and ENE-WSW oriented conjugate normal faults. Flat thrusts giving ENE directed shear may also be active under this field.3. A third stress field might be proposed with N-S compression and perpendicular extension directions. This would create NE-SW and NW-SE oriented shear fractures, which are observed in the measured fault data. It is remarkable that the NE-SW faults are all steep, subvertical, and give a very well defined fault set. Based on the fresh topographic expression, this stress field is also sub-recent.The different sub-recent stress fields and related fault patterns might succeed each other or might alternate through time. The first and third deformations have fresh topographic expressions and cannot play synchronously. The observed features suggest a compressionally active neotectonics of the study area. (c) 2005 Published by Elsevier B.V.

The Somogy hills are located in the Pannonian Basin, south of Lake Balaton, Hungary, above several important tectonic zones. Analysis of industrial seismic lines shows that the pre-Late Miocene substratum is deformed by several thrust faults and a transpressive flower structure. Basement is composed of slices of various Palaeo-Mesozoic rocks, overlain by sometimes preserved Paleogene, thick Early Miocene deposits. Middle Miocene, partly overlying a post-thrusting unconformity, partly affected by the thrusts, is also present. Late Miocene thick basin-fill forms onlapping strata above a gentle paleo-topography, and it is also folded into broad anticlines and synclines. These folds are thought to be born of blind fault reactivation of older thrusts. Topography follows the reactivated fold pattern, especially in the central-western part of the study area.The map pattern of basement structures shows an eastern area, where NE-SW striking thrusts, folds and steep normal faults dominate, and a western one, where E-W striking thrusts and folds dominate. Folds in Late Neogene are also parallel to these directions. A NE-SW striking linear normal fault and associated N-S faults cut the highest reflectors. The NE-SW fault is probably a left-lateral master fault acting during-after Late Miocene. Gravity anomaly and Pleistocene surface uplift maps show a very good correlation to the mapped structures. All these observations suggest that the main Early Miocene shortening was renewed during the Middle and Late Miocene, and may still persist.Two types of deformational pattern may explain the structural and topographic features. A NW-SE shortening creates right-lateral slip along E-W faults, and overthrusts on NE-SW striking ones. Another, NNE-SSW shortening creates thrusting and uplift along E-W striking faults and transtensive left-lateral slip along NE-SW striking ones. Traces of both deformation patterns can be found in Quaternary exposures and they seem to be consistent with the present day stress orientations of the Pannonian Basin, too. The alternation of stress fields and multiple reactivation of the older fault sets is thought to be caused by the northwards translation and counter-clockwise rotation of Adria and the continental extrusion generated by this convergence. (c) 2005 Elsevier B.V. All rights reserved.

Al/n-GaAs and Al/n-AlGaAs Schottky, junctions prepared on epitaxial layers grown by different methods, were studied by current-voltage and capacitance-voltage measurements as a function of temperature. It was concluded that the obtained anomalies of electrical behaviour are connected With the interaction of Al with GaAs and AlGaAs at temperatures as low as 500 degrees C.

Palaeomagnetic, palaeobiogeographic and structural comparisons of different parts of the Alpine-Carpathian region suggest that four terranes comprise this area: the Alcapa, Tisza, Dacia and Adria terranes. These terranes are composed of different Mesozoic continental and oceanic fragments that were each assembled during a complex Late Jurassic-Cretaceous Palaeogene history. Palaeomagnetic and tectonic data suggest that the Carpathians are built up by two major oroclinal bends. The Alcapa bend has the Meliata oceanic unit, correlated with the Dinaric Vardar ophiolite, in its core. It is composed of the Western Carpathians, Eastern Alps and Southern Alcapa units (Transdanubian Range, Bukk). This terrane finds its continuation in the High Karst margin of the Dinarides. Further elements of the Alcapa terrane are thought to be derived from collided microcontinents: Czorsztyn in the N and a carbonate unit (Tisza?) in the SE. The Tisza-Dacia bend has the Vardar oceanic unit in its core. It is composed of the Bihor and Getic microcontinents. This terrane finds its continuation in the Serbo-Macedonian Massif of the Balkans.The Bihor-Getic microcontinent originally laid east of the Western Carpathians and filled the present Carpathian embayment in the Late Palaeozoic-Early Mesozoic. The Vardar ocean occupied an intermediate position between the Western Carpathian-Austroalpine-Transdanubian-High Karst margin and the Bihor-Getic-Serbo-Macedonian microcontinent. The Vardar and Pindos oceans were opened in the heart of the Mediterranean-Adriatic microcontinent in the Late Permian-Middle Triassic. Vardar subducted by the end of Jurassic, causing the Bihor-Getic-Serbo-Macedonian microcontinent to collide with the internal Dinaric-Western Carpathian margin.An external Penninic-Vahic ocean tract began opening in the Early Jurassic, separating the Austroalpine-Western Carpathian microcontinent (and its fauna) from the European shelf. Further east, the Severin-Ceahlau-Magura also began opening in the Early Jurassic, but final separation of the Bihor-Getic ribbon (and its fauna) from the European shelf did not take place until the late Middle Jurassic.The Alcapa and the Tisza-Dacia were bending during the Albian-Maastrichtian. The two oroclinal bends were finally opposed and pushed into the gates of the Carpathian embayment during the Palaeogene and Neogene. At that time, the main NS shortening in distant Alpine and Hellenic sectors was linked by a broader right-lateral shear zone along the former Vardar suture. (C) 2004 Elsevier B.V. All rights reserved.

Paleomagnetic sampling was carried out in Mesozoic exposures of Northwest France and Southeast Belgium. Cretaceous localities in Hainaut, Boulonnais and Normandie yielded statistically well defined paleomagnetic directions. These localities fall into two groups. Hainaut and Boulonnais are characterized by declinations suggesting 30° counterclockwise (CCW) angular deviation of declination with respect to the present North, while Normandie exhibits moderate (12°) clockwise (CW) angular deviation with respect to the present North. In Normandie, we also observed occasionally very weak signals of a CCW deviated component, which, however, could not be treated statistically. Fold test suggests that both groups of samples were remagnetized during deformation. The overall mean paleomagnetic declination of the first group is westernly, that of the second group practically coincides with post-Eocene European reference directions, From assessing structural inversion and relevant paleostress-directions in Normandie, remagnetization may be connected to tectonic inversion in late Eocene-Oligocene times. While the statistically meaningful paleomagnetic result for the second group fit the synthetic stable European apparent polar wander path (APWP) at about 30 Ma, the overall mean paleomagnetic direction of the first group (based on 5 localities, representing 42 samples) defines a pole which is significantly offset from it, at any time following the deposition of the studied sediments. One explanation of this offset could be intraplate rotation on a small (Brabant Massif) scale. However, the angle of deviation in declination seems to be too large for a tectonic solution. Furthermore the data obtained from the Paleozoic do not show such declination deviation. It seems, therefore, that we need to increase considerably the direct stable European paleomagnetic database for the late Cretaceous-Tertiary, in order to further improve the late Cretaceous-Paleogene segment of the European APWP.

Three independent methods: paleomagnetic in- vestigation, analysis of reflection seismic sections and struc- tural study of outcrops have been applied to Mesozoic- Tertiary rocks of the Mecsek and VillMts (SW Hungary), which form inselbergs in the southern part of the Pannonian Basin. The structural history is marked by Late Oligocene- Early Miocene NW-SE shortening (in present cooridinates); late Early Miocene N-S shortening together with important clockwise rotations of the whole area and local counter- clockwise rotations in E-W left lateral wrench corridors; smaller N-S shortening with local wrenching and positive in- version during the Middle Miocene; an important N-S short- ening creating large folds and thrust reactivation in Late Miocene; a transtension characterised by roughly WNW- ESE elongation directions, creating left lateral oblique fault- ing along NE-SW oriented fault segments in Late Miocene; an important NW-SE shortening from latest Miocene to Present. This latter reactivated E-W structures as right lateral transpressive wedges and generated locally important rota- tions along them. Comparison of the obtained and regional structural data and rotation pattern strongly modifies our original concepts about microplate behaviour in the Intra-Carpathian realm. The geodynamic history is still dominated by the opposite rotation and consequent interplay of two major terranes: Al- capa and Tisza, but these are no more considered as rigid blocks. Differential rotations and deformations within Tisza are explained by major tears or thrusts across this block. Left lateral wrench zones within the clockwise rotating Tisza block are explained by differential movements due to this ro- tation. Both paleomagnetic and structural data indicate that the main phase of rotation and complex deformation was in Late Ottnangian (ca. 18 Ma), followed by a more quiescent period in this part of the Pannonian Basin. Several strong re- activations, perhaps with incipient rotation, are experienced from Late Miocene (ca. 11,5 and ca. 7 Ma) on.

Stratigraphic and structural investigations based on geological mapping in the Kis-fennsik region (NE part of the Bukk Mts, NE Hungary) proved the complex nappe structure of the area. According to new biostratigraphic data and structural setting, three main tectonostratigraphic units can be distinguished: in lowest structural position Carboniferous to Triassic deposits of the Bukk Parautochthonous Unit are forming a huge south-vergent anticline (North Bukk Anticline NBA). The Szarvasko-type Harica Nappe (HN, representing the upper part of the Jurassic) is thrust over the northern limb of the anticline. After the emplacement of the Harica Nappe, Middle-Upper Triassic rocks of the North Bukk Anticline (Szeleta sliver, NBA/b) are thrust onto the HN unit, and along an E-W striking thrust fault onto the older part of the NBA unit. In the southern part of the investigated area a narrow zone of platform carbonates and dark shales (Vesszos Formation) was mapped. Together with the overlying thick cherty limestone succession, they are considered to belong to the NBA/b unit. All the above mentioned units, affected by regional dynamothermal metamorphism, are overlain by the Kisfennsik Nappe (KN), which consists of slightly metamorphosed Carman platform limestones and dolomites, with some intercalating metavolcanites. Emplacement of the thrust sheet to the SE resulted in small- to mapscale folding in the North Bukk Anticline. Thrusting is attributed to the Cretaceous tectonometamorphic evolution of the Bukkium. Later, an intensive shortening generated well-developed, NE-SW oriented antiform-synform structures with reverse faults in all units. Folds with NW-SE axis represent another deformation phase.