Abstract

The structural setting and geological history of the eastern Iberian range and the Neogene basins are outlined. The following Neogene basins and structures are then reviewed: Calatayud–Daroca, Teruel, Serrion with Rubielos and Mijares, Eastern Maestrat, Alcora–Ribeselbes.

Introduction

During the Paleogene, the convergence of Iberia and Eurasia produced several major compressive structures in the inner part of the Iberian Plate, including the Iberian Chain. This NE–SW intraplate chain resulted from a tectonic inversion of Mesozoic extensional basins (Alvaro et al., 1979). The structure of this chain includes a Hercynian basement and a thick Mesozoic cover. A thick packet of Middle–Late Triassic mudstones and evaporites constitutes a detachment level which caused different structural responses in the Hercynian basement with its Permian–Early Triassic tegument, and the Jurassic–Cretaceous cover (Richter & Teichmuller, 1933; Viallard, 1989; Guimerá & Alvaro, 1990; Roca, 1992). The basement faults controlled the history of the Mesozoic basins (Alvaro et al., 1979).

The complex structure of this chain is determined by the diverse orientation of the basement faults in relation to the Paleogene compression direction. A transpressive strike–slip motion in the basement faults and a complex array of folds and thrusts in the cover were produced when the orientation of the basement faults was oblique to the regional shortening direction (N–S approximately). In these areas, the cover structures display a double vergence: to the NE in the northern part of the chain and to the SW in the southern part (Riba & Rios, 1962).