Publication: Discriminating between tectonism and climate signatures in palustrine deposits:
Lessons from the Miocene of the Teruel Graben, NE Spain
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Publication Date
2012
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Elsevier Science B.V., Amsterdam
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Abstract
The Upper Miocene (Vallesian–Turolian) Unit II of the Teruel Graben comprises at its top a 25 m-thick sequence
of palustrine deposits. Deposition of the entire unit commenced some 9 to 7 Ma ago in a halfgraben
basin. Here, via a recent quarry, we examine in detail the lateral and vertical distribution of Unit II's
palustrine facies and their features to determine the palaeogeography and main controls on deposit formation.
Our findings suggest the deposits formed at a low-gradient lake margin with different energy levels.
These energy levels controlled the type of primary deposit within the lake; wackestone to packstone sediments
formed in low-energy conditions, whereas cross-bedded rudstones to floatstones formed under higher
energy conditions, by erosion and redeposition of prior lacustrine deposits. Pedogenic and diagenetic modifications
of the primary sediments took place during sedimentary discontinuities (SD) when the lacustrine
sediments were subaerially exposed. These processes serve to explain the formation of eight different palustrine
limestones: limestones with root traces, mottled limestones, brecciated limestones, flat pebble breccias,
granular limestones, micro-karstified limestones with laminar calcretes, carbonate mounds and clayey limestones
with laminar calcretes. Based on the features and thicknesses of the modified sediments five different
morphological stages (I to V) of palustrine carbonates are defined. Stage I is characterized by incipient mottling
and brecciation. Stage II shows mottling and strong brecciation that lead to the formation of intraclast
breccias, in which the fragments are mostly “in situ”. In Stage III, the primary fabric is totally changed; intraclasts
have moved and may have lost their initial morphology. This Stage III may also be characterized by the
formation of micro-karst. Stage IV is typified by the presence of coated grains and thin root mats. The chronological
data available suggest that the formation of Stage III (lacustrine deposition+palustrine modification)
would require about 40,000 yr.
Facies and the SD record changes across short horizontal distances, and thus reflect the topography of prior
sedimentation/modification events. Small (50 cm) highs with micro-karst have their SD counterparts in
lower areas of the lake, in which the SD is indicated by desiccation and mottling. The topographic differences
of the micro-karst were filled by intraclastic rudstones sourced by the adjacent carbonate flats. The example
examined not only clearly sketches the morphology of ancient palustrine systems or wetlands, it also provides
evidence that recycling of previous carbonate deposits played an important role as a sediment source,
apart from biogenic or physical–chemical production processes.
Our geochemical data indicate LMC (Low Magnesian Calcite) as the main component and Fe contents lower
than 1%, except for the mottled areas that are richer in FeO. Stable isotope compositions provide δ18O values
close to −6.5‰ VPDB, and more varied δ13C (−3.39 to −6.97‰ PDB). Oxygen and carbon values reveal no
covariation and clear trends are lacking. The homogeneity of δ18O values reflects the intense effects of meteoric
waters.
The deposition of these palustrine limestones took place under suitable semi-arid to sub-humid climates. Climate
could also have a role in determining subaerial exposure periods. However, its imprint is not easy to detect
neither in the geochemical signals nor in the vertical arrangement of the facies. This could be attributed
to climate changes probably occurring over shorter periods than those that can be recorded in this type of
sediment, such as the astronomical precession cycles, and suggests the unsuitability of palustrine carbonates
for detailed palaeoclimate analyses.
Tectonism controlled the location of the main lacustrine depocentre close to the basin's main fault. The activity
of this normal fault during the sedimentation of Unit II determined long- and short-term sedimentary sequences.
Such sequences are the response to small-scale subsidence pulses followed by the infill of the
created accommodation space by shallow lacustrine deposits, which underwent early pedogenic and diagenetic
processes after subaerial exposure.