Corrigendum to: Links between foreland rheology and the growth and evolution of a young mountain belt in New Guinea
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Foreland basins are important areas of exploration for petroleum in China.According to the basin construction and evolution,the foreland basins in central and western China can be divided into four types of assemblages including the presenile,the reconstructed,the regenerated and the superimposed.This paper discusses the geological conditions of accumulation,such as the assemblages of source rock,reservoir and seal,in different foreland basins based on the examples of northwestern Junggar foreland basin(the presenile),western Sichuan foreland basin(the reconstructed),northern Chaidamu foreland thrust(the regenerated) and southern Junggar foreland basin(the superimposed).The thermal evolutions of main source rocks are stated in the four types of foreland basins.The foreland development in the late period of Himalayan movement has an obvious control on the thermal evolution of source rocks in the Chaidamu foreland thrust(the regenerated) and southern Junggar foreland basin(the superimposed).
Hydrocarbon exploration
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Abstract We use a Landscape Evolution Model including flexural isostasy to investigate the influence of inherited foreland relief on the stratigraphic evolution of the retro‐foreland domain during mountain building. We show models with four different types of initial relief in the foreland domain: at sea level, elevated (+300 m), a 1 km‐deep and 100 km‐wide foreland basin associated with either a forebulge at sea level or elevated at +300 m. During the first 10 Myr of simulation, the landscape evolution of the foreland is significantly altered by its inherited bathymetry/topography. The impact is then smoothed out once the foreland slope has stabilized and develops a transverse drainage network. Models record a long‐term shallowing‐up mega‐sequence driven by the increase in sediment production rate in the uplifting range and the decrease in the rate of flexural accommodation space creation in the foreland basin. The initial relief of the foreland domain alters the timing of its transition from the under‐filled to the over‐filled phase. An initially deep foreland basin is twice as thick as an initially elevated foreland. It records deep marine deposits while a foreland initially at sea level records thin shallow marine and an elevated foreland records continental deposits. The forebulge is buried by continental deposits in an initially elevated foreland while it is buried by marine sediments in other models. Alluvial fans at the foot of the range are more elevated in initially elevated forelands. We discuss our results of modeled stratigraphic architecture in comparison with the Pyrenean, Alpine and Andean retro‐foreland basins.
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The southern Alborz mountains of northern Iran are an integral part of the Arabia/Eurasia collision zone. A magnetostratigraphic and rock magnetic investigation of the Eyvanekey stratigraphic section in the southern Alborz mountains reveals the spatiotemporal character of sedimentary facies migration in the Alborz foreland basin. The section constitutes three coarsening upward units (units 1, 2, and 3), comprising the Upper Red and Hezardarreh formations. Our data reveal that the Upper Red Formation was deposited between 17.5 and 7.5 Ma, while the depositional age of the top of the Hezardarreh Formation can be extrapolated to ∼6.2 Ma. Slow sediment accumulation rates correlate with sedimentary facies comprising prograding, coarsening‐upward units. This is likely the result of intraforeland uplift (units 1 and 2) and basin inversion, probably associated with a growth syncline located in the proximal foreland (unit 3). In contrast, fine‐grained strata at the bottom of each cycle are associated with faster sediment accumulation rates, testifying to enhanced flexural basin subsidence in the course of thrust loading. Progradation of coarse‐grained facies also occurred during relatively fast sediment accumulation (top of unit 2), suggesting that the influx of coarse‐grained sediment outpaced the storage capacity of the proximal foreland. Thus, despite an overall southward propagation of deformation into the southern Alborz foreland, the locus of active deformation must have migrated back and forth on a time scale of circa 0.7 to 2 Ma.
Progradation
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Magnetostratigraphy
Isopach map
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The origin and evolution of the concepts, foreland, foreland basin and foreland basin system, are reviewed. Foreland is a relatively stable area near compressive mountain ranges which can be divided into three types, type - I , used to be passive continental margins, type-II ,associated with drench- arc systems and type- III, related to intra- continental mountain belts. A foreland basin can be defined as an elongate, deep depression along convergent mountain. Foreland basins can be classified as peripheral, retroarc and intra-continen-tal(or reactive) foreland basins. A foreland basin system is a system of basins developing along a convergent mountain, which can be divided into wedge top,foredeep,forebulge and back -bulge in a cross section.
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New guinea
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Abstract. We use two-dimensional thermo-mechanical models to investigate the potential role of rapid filling of foreland basins in the development of orogenic foreland fold-and-thrust belts. We focus on the extensively studied example of the Western European Alps, where a sudden increase in foreland sedimentation rate is well documented during the mid-Oligocene. Our model results indicate that such an increase in sedimentation rate will temporarily disrupt the formation of an otherwise regular, outward-propagating basement thrust-sheet sequence. The basement thrust active at the time of a sudden increase in sedimentation rate remains active for a longer time and accommodates more shortening than the previous thrusts. As the propagation of deformation into the foreland fold-and-thrust belt is strongly connected to basement deformation, this transient phase appears as a period of slow migration of the distal edge of foreland deformation. The predicted pattern of foreland-basin and thrust-front propagation is strikingly similar to that observed in the North Alpine Foreland Basin and provides an explanation for the coeval mid-Oligocene filling of the Swiss Molasse Basin, due to increased sediment input from the Alpine orogen, and a marked decrease in thrust-front propagation rate. We also compare our results to predictions from critical-taper theory and we conclude, that they are broadly consistent, although, when sedimentation is included, critical-taper theory cannot be used to predict the timing and location of the formation of new basement thrusts. The evolution scenario explored here is common in orogenic foreland basins; hence our results have broad implications for orogenic belts other than the Western Alps.
Basement
Sedimentation
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<p>Foreland basins record the evolution of orogens through sedimentary accumulation and recycling and, as such, represent unique archives of the evolution of orogenic systems. Foreland basins are, however, complex source-to-sink systems responding to the uplift of the mountain range, thrusting, eustasy, climate, and the type of lithologies eroded. The respective contributions of these parameters has been numerically evaluated, the influence of the inherited geometries of the foreland on the sediment routing systems has not yet been investigated.</p><p>We use a Landscape Evolution Model (FastScape) to explore the effect of varying foreland paleo-topography on its stratigraphic architecture. Models consist of a half mountain range steadily uplifting (0.5 mm/yr) over 25 Myrs. Eroded material is transported and deposited in a foreland domain and a distal open marine domain. We present 4 setups with varying paleo-topographies in the foreland domain: an initial flat foreland at sea level (M1), an elevated flat continental foreland (+300 m, M2), a pre-existing 1 km-deep and 100 km-wide depression at the foot of the growing orogen with either a flat forebulge at sea level (M3) or an elevated forebulge (+300m; M4).</p><p>Our result show that an elevated foreland domain produces, after 25 Myrs, a thinner foreland basin because the faster and efficient sediment export of sediment out of the foreland to the open marine domain reduces the sedimentary load and, in doing so, the flexure. In contrast, a pre-existing depression at the foot of the range, produces a thicker foreland basin because the additional load filling the initial space increases the flexural response. We show that a pre-existing bathymetry is required to preserve marine deposits in the foreland basin. In our experiments, the landscape after 25 Myrs cannot be used to infer the initial foreland geometry as the initial foreland influences is smoothed out after ~10-15 Myrs. The stratigraphic architectures of the foreland basin are nonetheless different. In addition, we show that emplacement of an alluvial fan at the foot of the range results in a transient drop in erosion rate in the range by locally increasing the base-level (autogenetic feedback).</p>
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