An overview of tectonosedimentary framework of the Salt Range, northwestern Himalayan fold and thrust belt, Pakistan

Ghazi, Shahid; Ali, Syed Haroon; Sahraeyan, Mohammad; Hanif, Tanzila

doi:10.1007/s12517-014-1284-3

Cited by 34 publications

(18 citation statements)

References 37 publications

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“…Simplified geologic map of the study area. Constructed after: CALKINS & OFFIELD (1974), GEE (1980), DIPIETRO et al (2008), GHAZI et al (2014), JADOON et al (2015), GHANI et al (2018). Kalabagh and Jhelum faults traced after KAZMI & RANA (1982) runs mostly along a sharp topographic boundary, opposing non-metamorphic Meso zoic-Palaeogene rocks in hilly terrain to mostly Mio-Plio cene molasse sediments in the southern lowlands, plateaus.…”

Section: Regional Geological Frameworkmentioning

confidence: 99%

“…The salt formation is overlain by a sequence of Cambrian continental-shallow marine formations including sandstones and dolostones. The Cambrian formations can be 500-100 m thick (thickness being modified by salt tectonics; GHAZI et al 2014).…”

Section: General Stratigraphymentioning

confidence: 99%

“…After a long break in sedimentation and an unconformity, Permian glacial sandstones, tillites and conglomerates, then carbonates are deposited, to be followed by an apparently concordant sequence of Triassic-Jurassic-Creta ceous rocks (GHAZI et al 2014). The individual formations may follow local hiatuses.…”

Section: General Stratigraphymentioning

confidence: 99%

“…This unconformity probably indicates the first collision episode of the Indian margin with the Kohistan arc (TREOLAR et al 1992). It erodes sediments towards the SE, so the Mesozoic and partly the Permian are missing in SE Potwar (GHAZI et al 2014). The unconformity is overlain by sandstone, limestone and deep marine shale-marl deposited in a foredeep basin.…”

Section: General Stratigraphymentioning

confidence: 99%

“…Again a major break and an unconformity is observed at the top of Eocene (Figure 3). (Oligocene)-Miocene-Pliocene-Pleistocene continental sediments are deposited locally in huge thickness (in excess of 6-7 km) on top of the older formations (GHAZI et al 2014). Most of these sandstonesshales-conglomerates have fluvial origin and gradually fill up the subsiding Himalayan foredeep.…”

Section: General Stratigraphymentioning

confidence: 99%

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Transversal folding in Himalaya foothill ranges

Csontos¹,

Dunkl

Vakarcs

et al. 2019

Földt. Közl.

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The Himalayan foreland in N Pakistan, dissected by Main Frontal Thrust (MFT) and Main Boundary Thrust (MBT) contains spectacular salients and syntaxes. The lateral (N-S) boundaries between these salients and syntaxes around Kalabagh city and east-southeast of Islamabad were believed to host deep-seated lateral ramps with strike slip movements. However, seismic data in these two sectors suggest that there are N-S trending folds and locally east- or west-vergent thrusts that affect the Paleozoic-Paleogene cover of the Indian shield, as well as the Miocene-Pliocene molasse sediments. The proposed lateral ramps cannot be followed on the seismic and on maps either; instead, both maps and seismic data suggest folding, often on a regional scale of harder Paleo-Mesozoic-Paleogene and softer Oligo-Miocene-Pilo-Pleistocene cover. The NE corner of Surghar range is proposed to be formed of relaying thrust sheets with emergent heads composed of Paleozoic-Paleogene and its slightly detached Miocene molasse. These relaying imbricates are taken in a southward flexure generated by a major right lateral shear of a wide zone, where transpressive Riedel shears, en echelon anticlines and southwards flexed earlier thrust faults are the main elements (but a single, through-going Kalabagh fault is missing). The generation of mapped N-S trending folds and east-vergent thrusts preceded the formation of the wide shear zone and southwards flexing.Hazara syntaxis is interpreted as a major antiform that re-folded MBT and Panjal thrust around Oligo-Miocene molasse, itself forming an antiform (BOSSART ET AL. 1988). In our model we propose that the west-vergent Balakot thrust and deeper blind thrusts are in the core of this antiform. In the southern continuation we propose that folds in Miocene molasse continue from eastern Potwar region to western Kashmir and there appears no major break. These structures are also re-folded in a major antiform with N-S axial trend. Map analysis also suggests that N-S trending folds bending earlier main thrusts are occurring in a wide area south of the Indus-Tsangpo suture.Several independent geological and geophysical observations including mapping, seismic analysis, earlier measurements of strain axes and of paleomagnetic declinations suggest that the salients and syntaxes may have been much more linear in the past (although a total linearity is not realistic). It is proposed that the present-day undulating pattern may have been generated by N-S trending folds due to general (and episodic) E-W shortening. If the main fault zones were more linear, the relay pattern along their segments suggests a left lateral shear component along MBT and a mixed, locally left, locally right lateral component along MFT. Earlier (ZEITLER 1985) and now provided low temperature thermochronological ages strongly suggest a rather general episode of E-W shortening between 4-5 Ma for the whole northern Indian margin. However, there should have been original transversal dome formation as early as Oligocene (DIPIETRO ET AL. 2008). It is also clear that longer N-S shortening and shorter E-W shortening episodes should alternate eventually in a very short time frame, since earthquake focal mechanisms (LISA AND KHWAJA 2004, BURG ET AL. 2005) suggest the coexistence of E-W compression and NW-SE compression in Potwar.There are several potential explanations for generating E-W shortening and related structures in a general N-S shortening regime. Possibilities range from fault terminations of thrust faults at high angles in a particular zone (TREOLAR ET AL. 1992) to en echelon folding along a major right lateral E-W fault zone. However, we speculate that E-W shortening could be much more general, suggesting a mechanism that affects the whole of Indian plate. Possibly the best explanation is given by analogue models (REPLUMAZ ET AL. 2012) proposing major, slightly convergent confining boundaries. If applied to the northwards advance of India, the northwards converging boundaries generate secondary E-W shortening and east-or west-vergent orogens parallel to these boundaries.

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Section: Regional Geological Frameworkmentioning

confidence: 99%

Section: General Stratigraphymentioning

confidence: 99%

Section: General Stratigraphymentioning

confidence: 99%

Section: General Stratigraphymentioning

confidence: 99%

Section: General Stratigraphymentioning

confidence: 99%

See 3 more Smart Citations

Transversal folding in Himalaya foothill ranges

Csontos¹,

Dunkl

Vakarcs

et al. 2019

Földt. Közl.

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A multi‐proxy based high‐resolution stratigraphical analysis of the possible Palaeocene–Eocene boundary interval, Salt Range, Pakistan

et al. 2020

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The Palaeocene–Eocene boundary (PEB) interval has been recognized in the Patala Formation, Nammal Gorge Section, Pakistan using lithostratigraphy, stable carbon isotope stratigraphy and integrated biostratigraphy. Four distinct lithological units are identified in the Patala Formation in stratigraphic order from bottom to top; unit‐1 to unit‐4. The top of unit‐3 hosts three closely spaced unconformities demarcated as U1, U2, and U3. The PEB interval is represented by a negative shift of 1.61‰ in δ13CV‐PDB representing the carbon isotopic excursion (CIE) in unit‐2. Based on the encountered foraminifera, dinocysts, and calcareous nannoplanktons, the following biozones are identified across the PEB; two larger benthonic foraminiferal (LBF) zones (SBZ4 and SBZ5), the zonal boundary slightly postdating the CIE, two smaller benthonic foraminiferal zones (BB1 and BB2), three planktonic foraminiferal zones (P4/P5 + E1), four dinocysts zones (Pak‐DV, Pak‐DVI, Pak‐DVII, Pak‐DVIII), and two calcareous nannoplankton subzones (NP9a and NP9b). The following protist, dinocyst and calcareous nannoplanktons encountered in the studied interval advocates for the placement of the possible PEB at the level between samples NAM‐SH‐07 and 08; 1—presence of the smaller benthonic foraminifera Angulogavelinella avnimelechi diagnostic of the base of the CIE and the benthonic extinction event (BEE) Tethys wide, 2—presence of the cosmopolitan and the PEB diagnostic dinocyst species ‘Axiodinium augustum’, 3—presence of the PEB diagnostic Rhomboaster‐Discoaster calcareous nannoplankton assemblage. The LBF species Alveolina vredenburgi [a marker species of the Larger Foraminiferal Turnover (LFT) associated with the Palaeocene Eocene Thermal Maximum (PETM) and PEB in western Tethys] occurs slightly above the onset of the CIE. Previously reported compositional change in the LBF assemblage from the Salt Range [i.e. the replacement of the Palaeocene orbitoidiform LBF (Setia and Orbitosiphon) by the Eocene LBF (Orthophragminids, Alveolina, Nummulites and Assilina)] also postdates the PEB interval here. The late appearance of Alveolina vredenburgi and the compositional change in the LBF after the onset of the CIE are attributed to the facies variation across the PEB reflecting fluctuating depositional environment due to the active tectonic across this interval. This fluctuation is evident from the smaller benthonic and planktonic foraminiferal dominating assemblages in unit‐2 representing bathyal settings followed by LBF dominating unit‐3 representing shallow carbonate platform settings. The change in LBF assemblage closely resembles the well‐known LFT associated with the PETM as well as the carbonate platform stage III and the PEB reported from other Tethyan sections.

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