Interplay between longitudinal fluvial and transverse alluvial fan systems and growing thrusts in a piggyback basin (SE Pyrenees)

Ramos, Emilio; Busquets, Pere Solà; Vergés, Jaume

doi:10.1016/s0037-0738(01)00169-5

Cited by 35 publications

(42 citation statements)

References 32 publications

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“…The age of this reverse faulting in the Axial Zone of the Pyrenees is in agreement with previous geochronological data on the Têt fault (Sère 1993) and Merens fault (McCaig and Miller 1986;Majoor 1988;Maurel 2003;Maurel et al 2004b), with thermochronological data in Central Pyrenees (Fitzgerald et al 1999) and with sedimentological data from the southern flank of the Pyrenean range (Burbank et al 1992;Déramond et al 1993;Vergès and Burbank 1996;Ramos et al 2002).…”

Section: Geodynamical Conclusionsupporting

confidence: 90%

The Meso-Cenozoic thermo-tectonic evolution of the Eastern Pyrenees: an 40Ar/39Ar fission track and (U–Th)/He thermochronological study of the Canigou and Mont-Louis massifs

Maurel¹,

Monié²,

Pik³

et al. 2007

Int J Earth Sci (Geol Rundsch)

120

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Vertical displacements on the SW-NE Têt fault (Eastern Pyrenees Axial Zone, France), which separates the Variscan Canigou-Carança and Mont-Louis massifs, were constrained using a thermochronologic multi-method approach. 40 Ar/ 39 Ar data from the granitic Mont-Louis massif record its Variscan cooling history and reveal no ages younger than Early Cretaceous, while the CanigouCarança gneiss massif records systematically younger 40 Ar/ 39 Ar ages. These younger 40 Ar/ 39 Ar ages in the Canigou-Carança gneiss massif are the result of partial to total rejuvenation of argon isotopic systems related to a thermal flow coeval with the Cretaceous HT-BP metamorphism in the North Pyrenean Zone. Only the deepest rocks from the Canigou-Carança suffered this extensive Mid-Cretaceous thermal overprint probably due to differential burial around 4 km at that time. The post Mid-Cretaceous vertical displacements along the Têt fault are recorded by ''low'' temperature thermochronology using K-feldspar 40 Ar/ 39 Ar, zircon and apatite fission track and (U-Th)/He datings. The Mont-Louis granite samples experienced a long period of protracted cooling reflecting a lack of thermo-tectonic activity in this area from Late Palaeozoic to Early Cenozoic, followed by cooling from 55-60 Ma to Late Eocene at a mean rate of 15-20°C/Ma in the final stage. This cooling stage corresponds to Têt fault reactivation with a reversed component, promoting exhumation of the Mont-Louis roof zone contemporaneously with the south-vergent Pyrenean thrusting. In the CanigouCarança massif, the main cooling event occurred from 32 to 18 Ma at a maximum rate of 30°C/Ma during Early Oligocene followed by a more moderate rate of 3°C/Ma from Late Oligocene to Early Burdigalian, coeval with the normal reactivation of the Têt fault in brittle conditions that accommodated the final exhumation of the massif during the opening of the Gulf of Lion.

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Section: Geodynamical Conclusionsupporting

confidence: 90%

The Meso-Cenozoic thermo-tectonic evolution of the Eastern Pyrenees: an 40Ar/39Ar fission track and (U–Th)/He thermochronological study of the Canigou and Mont-Louis massifs

Maurel¹,

Monié²,

Pik³

et al. 2007

Int J Earth Sci (Geol Rundsch)

120

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“…The columns are arranged in depositional dip-oriented trending approximately from east (proximal) to west (distal). The lithofacies columns display vertical succession of facies and facies associations similar to that employed by Rasmussen (2000) and Ramos et al (2002).…”

Section: Methods and Datamentioning

confidence: 70%

Stratigraphic Architecture and Lithofacies Analysis: Evidence for Development of the Pliocene-Holocene Taichung Foreland Basin, Central Taiwan

Kao¹,

Hong²,

Yu³

et al. 2013

Terr. Atmos. Ocean. Sci.

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The Taichung foreland basin, sub-basin of the Taiwan foreland basin, has developed since Pliocene. We studied stratigraphic architecture and the lithofacies of the Taichung basin in detail. We recognized eleven lithofacies, which are grouped into ten facies associations. Based on facies association analysis, we suggest that the development of the Taichung basin can be divided into four stages accompanied by syn-depositional deformation characterized by westward propagating thrust faults.Prior to 2.78 Ma, the basin was characterized by offshore environment during underfilled stage. Later, the Shuangtung Fault located to the east of the Western Foothills began to thrust westward and uplifted the Tertiary strata, which supplied sediments to basin between the Shuangtung and Chelungpu faults in initial filled stage. About 1 Ma, the Chelungpu Fault started to thrust westward and uplifted the Western Foothills, which shed fluvial sediments to fill basin between the Chelungpu and Tachia faults. After 0.46 Ma, the Tachia Fault began to thrust westward and strata immediately to the east of the Tachia Fault were uplifted to form ramps, producing Houli and Tatushan tablelands. The basin-filling reached the overfilled stage when the Chingshui Coastal Plain is dominated with fluvial facies.The Taichung foreland basin is bounded by Tachia and Shuangtung faults with the Chelungpu Fault in the middle and formed by active, sequentially propagating westward thrust faults from Pliocene to Pleistocene. The youngest Tachia Fault carried the piggyback basin in front of the older Chelungpu Fault, representing similar style to piggyback basins of the Po Basin and the Ebro Basin in Europe.

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“…Puigdefàbregas et al, 1992). The South Pyrenean foreland basin was partitioned into two different segments, both connected to the Atlantic during the early and middle Eocene: the Ripoll basin in the east (see a discussion in Nijman (1989) and Ramos et al (2002), and the Tremp-Pamplona basin in the west (Puigdefàbregas, 1975;Turner, 1992;Fig. Burbank et al, 1992a;Hogan & Burbank, 1996;Vergés et al, 1998).…”

Section: Ancient Examples From the Southern Pyreneesmentioning

confidence: 99%

Drainage Responses to Oblique and Lateral Thrust Ramps: A Review

Vergés

2007

Sedimentary Processes, Environments and Basins

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The relationships between oblique or lateral ramps in fold-and-thrust belts and their impact on syntectonic fluvial drainage are analysed in this review. Both ancient and recent cases from Cenozoic belts are examined. The southern flank of the Pyrenees provides good examples to decipher the long-term effects of oblique ramps on fluvial arrangement. Recent examples from the Indus River across the front of the Himalayas in northwest Pakistan, the frontal domains of the Andes in Bolivia and the northwest Zagros Mountain Belt provide examples of the short-term interaction between oblique or lateral thrust ramps and foreland drainage systems. The interpretation of these case studies, some of them developed on top of blind thrust ramps, can facilitate the analysis of drainage distortions in active complex tectonic regions.Oblique ramps are present either permanently or episodically at different scales in all fold-andthrust belts. The simplest scenario is related to piggyback basins, which display an oblique ramp linked to each frontal thrust termination. This oblique ramp forms the natural outlet for confined longitudinal systems along the piggyback basin. The change in topography across the ramp constrains the position of deltaic deposits between a subaerial fluvial system deposited in its hangingwall and an open marine system deposited in its footwall. Fluvial systems can also develop either in the hangingwall or in the footwall of larger oblique ramps that grow by the tectonic inversion of earlier structures. The growth of a large oblique ramp beneath a fluvial system operates in the same way as oblique ramps related to piggyback basins. However, its larger scale causes a larger differential topographic elevation across it, accommodating fluvial deposits in its hangingwall and deep marine turbidites in its footwall. In opposition, large oblique ramps growing in front of river systems create a topographic barrier that deflects the drainage.A complication of the interaction of oblique ramps and drainage occurs where two opposed oblique ramps form a tectonic reentrant. These tectonic reentrants form at different scales and are characterized by lower topography. The confined domains concentrate rivers flowing out from surrounding higher topographic deformed regions. Further development of deeper thrusts can uplift these reentrants, modifying the previous concentrated drainage and diverting the river courses towards regions with lower topography.As an example, the late Miocene longitudinal fluvial system flowing along the foreland basin of the Zagros during the deposition of the lower Agha Jari Formation was shifted to the southwest in the earliest Pliocene by the uplift of the Pusht-e Kuh Arc. The present river configuration is incising through the Pusht-e Kuh Arc anticlines and flows towards the lowlands of the Dezful Embayment (tectonic reentrant), limited by two major oblique ramps along the Mountain Front Flexure. The large-scale Mountain Front Flexure confines the Tigris River towards the southwest of the front of ...

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Interplay between longitudinal fluvial and transverse alluvial fan systems and growing thrusts in a piggyback basin (SE Pyrenees)

Cited by 35 publications

References 32 publications

The Meso-Cenozoic thermo-tectonic evolution of the Eastern Pyrenees: an 40Ar/39Ar fission track and (U–Th)/He thermochronological study of the Canigou and Mont-Louis massifs

The Meso-Cenozoic thermo-tectonic evolution of the Eastern Pyrenees: an 40Ar/39Ar fission track and (U–Th)/He thermochronological study of the Canigou and Mont-Louis massifs

Stratigraphic Architecture and Lithofacies Analysis: Evidence for Development of the Pliocene-Holocene Taichung Foreland Basin, Central Taiwan

Drainage Responses to Oblique and Lateral Thrust Ramps: A Review

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