The inner sector of the Eastern Carpathians displays a large number of Na-HCO3, CO2-rich, meteoric-originated cold springs (soda springs) and bore wells, as well as dry mofettes. They border the southern part of the Pliocene-Quaternary Calimani-Gurghiu-Harghita (CGH) calc-alkaline volcanic chain. Both volcanic rocks and CO2-rich emissions are situated between the eastern part of the Transylvanian Basin and the main east Carpathian Range, where active

The Miocene magmatism of the Apuseni Mountains in the Carpatho-Pannonian area hosts some of Europe's largest porphyry epithermal Cu-Au ore systems associated with shallow subvolcanic intrusions. Detailed field observations combined with K-Ar ages, geochemical analyses, Sr-Nd isotopes and paleomagnetic data constrain a model for the geotectonic evolution and processes of melt generation that may account for the exceptional mineralizing potential of

In the Carpathian–Pannonian region in Neogene times, westward-dipping subduction in a land-locked basin caused collision of two lithospheric blocks (Alcapa and Tisia) with the southeastern border of the European plate. Calc-alkaline and alkaline magmatism was closely related to subduction, rollback, collision and extension. From the spatial distribution of the magmatic activity, four segments can be defined: Western Segment (magmatism occurring

Mafic alkalic volcanism was widespread in the Carpathian–Pannonian region (CPR) between 11 and 0.2 Ma. It followed the Miocene continental collision of the Alcapa and Tisia blocks with the European plate, as subduction-related calc-alkaline magmatism was waning. Several groups of mafic alkalic rocks from different regions within the CPR have been distinguished on the basis of ages and/or trace-element compositions. Their trace element and Sr–Nd–Pb

K-Ar ages of rocks from the Gurghiu Mountains, the middle part of the longest volcanic chain in the Eastern Carpathians (Cãlimani–Gurghiu–Harghita), indicate an interval of volcanic activity between 9.4–5.4 Ma. Magmatic activity migrated from North to South and built the following volcanic centres: Jirca (J), Fâncel-Lãpusna (FL), Bacta (B), Seaca-Tãtarca (ST), Borzont (BZ), Sumuleu (S) and Ciumani-Fierãstraie (CF). The timing of volcanic

New K-Ar ages combined with paleomagnetic data demonstrate that the basaltic volcanism in the Persani Mountains occurred in two relatively short phases. The first one lasted several tens of thousands of years around 1.2 Ma and it seems that the inception of the volcanic activity took place in two isolated places and reached the maximum extent during the Cobb Mountain Normal Polarity Subchron when larger areas were covered. The second phase started

The Cãlimani Mountains represent the largest and most complex volcanic structure at the northern part of the Cãlimani–Gurghiu–Harghita range in Romania. Sixty-eight K-Ar ages (thirty-three new) provide constraints on the eruptive history of the Cãlimani volcanic structure between 11.3 and 6.7 Ma. The oldest rocks are from shallow exhumed intrusions, which pierced the basement between 11.3–9.4 Ma. The oldest stratovolcano was centered on

Neogene to Quaternary volcanism in the Carpathian-Pannonian Region was related to the youngest evolutionary stage of the Carpathian arc and the intra-Carpathian area, with subduction, extension and asthenospheric upwelling as the main driving mechanisms. Volcanism occurred between 21 and 0.1 Ma, and showed a distinct migration in time from West to East. Several groups of calc-alkaline magmatic rock-types (felsic, intermediate and mafic varieties)

A series of small Miocene (8.3–6.7 Ma) lamproite rock occurrences (as monogenetic volcanoes and/or dykes) cover a large area in southeastern Spain. These rocks are associated with extensional basins filled by Neogene deposits in the Betic and Subbetic structural units. At Cancarix (Sierra de las Cabras), Calasparra, Barqueros, Cerro de Monagrillo, Jumilla, and Vera, eruptions occurred, whereas at Fortuna, Mula and Zeneta there were only small-scale