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The Teruel Basin is a NNE-SSW trending intracontinental extensional basin located in centraleastern Iberia. It is asymmetrically bounded to the east by a major fault zone, but intrabasinal faults with diverse orientation (NNE-SSW to NE-SW, E-W, or NW-SE) also appear. Offsets of the successive sedimentary units and of two planation surfaces reveal that tectonic activity initiated at the border faults, while intrabasinal ones mainly developed in a later stage. Fractures on a map scale show a prevailing N-S strike in Neogene synrift rocks, while a dense network made of four main fracture sets (NE-SW, E-W to ESE-WNW, N-S and NNW-SSE), likely inherited from Mesozoic rifting stages, is observed in pre-rift units. The results of palaeostress analyses indicate an overall predominance of σ 3 directions around E-W, although two stress

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Alluvial fans and shallow carbonate lakes interfered in the Teruel half‐graben during the Late Miocene–Pliocene. Tectonic influence is recorded in alluvial and lacustrine–palustrine successions, with long‐term climate changes being recorded in detail in the isotopic signatures of carbonates. Episodes of tectonic activity induced alluvial fan progradation and lake retraction in the whole basin. Three lacustrine stages have been identified, which support the idea that climate also exerted an important control on sedimentation. The transition between stages 1 and 2 occurred during a tectonically calm episode due to an increase in aridity in the Early Turolian; small fans with source areas next to the lake margin prograded, inducing lake‐shore retraction. The transition from stage 2 to 3 was caused by the superimposition of increasing tectonic activity and aridity effects. Our study demonstrates that discrimination of allogenic factors controlling sedimentation in continental closed basins is possible using sequence stratigraphy in combination with other techniques such as geochemistry of carbonates.

This work describes soft-sediment deformation structures (clastic dykes, load structures, diapirs, slumps, 21 nodulizations or mudcracks) identified in three sections (Concud, Ramblillas and Masada Cociero) in the Iberian 22 Range, Spain. These sections were logged from boreholes and outcrops in Upper Pliocene-Lower Pleistocene de-23 posits of the Teruel-Concud Residual Basin, close to de Concud normal fault. Timing of the succession and hence 24 of seismic and non-seismic SSDSs, covering a time span between~3.6 and~1.9 Ma, has been constrained from 25 previous biostratigraphic and magnetostratigraphic information, then substantially refined from a new 26 magnetostratigraphic study at Masada Cociero profile. Non-seismic SSDSs are relatively well-correlated between 27 sections, while seismic ones are poorly correlated except for several clusters of structures. Between 29 and 35 28 seismic deformed levels have been computed for the overall stratigraphic succession. Factors controlling the lat-29 eral and vertical distribution of SSDSs are their seismic or non-seismic origin, the distance to the seismogenic 30 source (Concud Fault), the sedimentary facies involved in deformation and the observation conditions (borehole 31 core vs. natural outcrop). In the overall stratigraphic section, seismites show an apparent recurrence period of 56 32 to 108 ka. Clustering of seismic SSDSs levels within a 91-ka-long interval records a period of high paleoseismic 33 activity with an apparent recurrence time of 4.8 to 6.1 ka, associated with increasing sedimentation rate and 34 fault activity. Such activity pattern of the Concud Fault for the Late Pliocene-Early Pliocene, with alternating 35 periods of faster and slower slip, is similar to that for the most recent Quaternary (last ca. 74 ka BP). Concerning 36 the research methods, time occurrence patterns recognized for peaks of paleoseismic activity from SSDSs in 37 boreholes are similar to those inferred from primary evidence in trenches. Consequently, apparent recurrence 38 periods calculated from SSDS inventories collected in borehole logs close to seismogenic faults are comparable 39 to actual recurrence times of large paleoearthquakes.