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Petrogenesis of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan: Provenance, tectonic, and climatic implications
Accepted Manuscript Petrogenesis of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan: provenance, tectonic, and climatic implications Belal S. Amireh PII: DOI: Reference:
S1367-9120(17)30709-5 https://doi.org/10.1016/j.jseaes.2017.12.037 JAES 3369
To appear in:
Journal of Asian Earth Sciences
Received Date: Revised Date: Accepted Date:
2 July 2017 25 December 2017 27 December 2017
Please cite this article as: Amireh, B.S., Petrogenesis of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan: provenance, tectonic, and climatic implications, Journal of Asian Earth Sciences (2017), doi: https://doi.org/10.1016/j.jseaes.2017.12.037
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Petrogenesis of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous siliciclastic
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sequence of Jordan: provenance, tectonic, and climatic implications
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Belal S. Amireh
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Dept. of Applied and Environmental Geology
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The University of Jordan
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Amman 11942, Jordan
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[email protected]
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ABSTRACT
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Detrital framework modes of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous
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siliciclastic sequence of Jordan are determined employing the routine polarized light microscope.
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The lower part of this sequence constitutes a segment of the vast lower Paleozoic siliciclastic
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sheet flanking the northern Gondwana margin that was deposited over a regional unconformity
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truncating the outskirts of the East African orogen in the aftermath of the Neoproterozoic
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amalgamation of Gondwana. The research aims to evaluate the factors governing the detrital
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light mineral composition of this sandstone. The provenance terranes of the Arabian craton
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controlled by plate tectonics appear to be the primary factor in most of the formations, which
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could be either directly inferred employing Dickinson‘s compositional triangles or implied
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utilizing the petrographic data achieved and the available tectonic and geological data. The
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Arabian-Nubian Shield constitutes invariably the craton interior or the transitional provenance
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terrane within the NE Gondwana continental block that consistently supplied sandy detritus
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through northward-flowing braided rivers to all the lower Paleozoic formations. On the other
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hand, the Lower Cretaceous Series received siliciclastic debris, through braided-meandering
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rivers having same northward dispersal direction, additionally from the lower Paleozoic and
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lower-middle Mesozoic platform strata in the Arabian Craton. The formations making about
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50% of the siliciclastic sequence represent a success for Dickinson‘s plate tectonics-provenance
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approach in attributing the detrital framework components primarily to the plate tectonic setting
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of the provenance terranes. However, even under this success, the varying effects of the other
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secondary sedimentological and paleoclimatological factors are important and could be crucial.
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The inapplicability of this approach to infer the appropriate provenance terranes of the remaining
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formations could be ascribed either to the special influence of local intracratonic syn-rift
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rhyolitic extrusions, where their plate tectonic setting is not represented by the standard plate
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tectonics-provenance diagrams, or to the rather unusual effect of the Late Ordovician glacial
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event.
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Key words: Framework modes, provenance terranes, Gondwana, Arabian-Nubian Shield, lower
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Paleozoic siliciclastic platform, Jordan, sandstone types
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1. Introduction
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The modal framework composition of siliciclastic sediments and sedimentary rocks is governed
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by several factors including: provenance type, tectonic setting in general and plate tectonics in
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particular, climate and the corresponding type of weathering, mixing of sediments from multiple
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sources, mechanical modifications during transportation, effects of depositional environment,
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and influence of diagenesis generally and intrastratal solution particularly.
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Several publications considered the plate tectonic setting of the provenance the primary
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factor governing the modal framework composition of sandstone (Dickinson and Suczek, 1979;
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Dickinson et al., 1983; Dickinson, 1985, 1988). Other studies confirmed this plate tectonic-
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provenance approach. For instant, Marsaglia and Ingersoll (1992) documented that this model
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works excellently for magmatic arcs. In addition, Ingersoll and Eastmond (2007), and Ingersoll
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(2012) tested Dickinson's petrologic model relating sandstone composition to the dissected
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magmatic arc provenance, employing modern sands from Sierra Nevada drainages, and
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concluded the robust nature of the plate tectonic-provenance axiom.
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On the other hand, some studies criticized Dickinson‘s standard provenance approach,
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and highlighted inconsistent relationship, or disagreement between the modal framework
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composition of some sandstones with the plate tectonic setting inferred by the model (Suttner et
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al., 1981; Mack, 1984). This criticism was limited earlier to specific exceptions, such as
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derivation of clastics from an older tectonic setting, sandstone subjected to intensive weathering
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giving rise to super- or mature sandstone, mixing of two or more provenances or derivation from
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another tectonic setting not represented in the plate tectonic-provenance diagrams, and
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sandstones containing large amounts of detrital carbonate grains (Zuffa, 1985). Therefore, these
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sedimentary petrology schools refused to adopt Dickinson’s petrographic model and focused
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more on the compositional modifications during erosion, transport, deposition, and diagenesis.
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Another criticism to Dickinson‘s model is its establishment mainly upon ancient sandstones,
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where ancient plate tectonic settings, particularly those of the late Ediacaran Epoch, are assumed
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rather than known. Additionally, Weltje (2006) showed that the inferred continental block,
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magmatic arc, and recycled orogenic provenance terranes can be discriminated by Dickinson‘s
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model with a success rate of only 64% to 78%.
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Recently, Garzanti (2016) questioned the validity of inferring plate tectonic setting
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straightforwardly from the models of framework modes of sands and sandstones. It is recorded
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that the detrital modes of sandstones cannot decipher the plate-tectonic setting in which they
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were deposited because petrography alone cannot discriminate allochthonous versus
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autochthonous, orogenic versus anorogenic, or young versus old source rocks. Additionally,
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more substantial flaws were proposed, such as the oversimplification of orogenic domains and
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the disregard of rift related settings, anorogenic volcanism, and ophiolitic sources. Thus, it is
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concluded that the geodynamic setting could not be univocally inferred from the detrital modes
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of sandstone.
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The uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan, the lower
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part of which constitutes a segment of the immense lower Paleozoic siliciclastic platform
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bordering most of northern Gondwana margin, represents a unique case study to evaluate the
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weight of each of the various factors governing the detrital framework composition of sandstone.
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This is due to the high thickness of the sequence (ca 2500 m), and the immense geologic time
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represented spanning from the late Ediacaran to the Late Cretaceous. Moreover, various sorts of
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provenance terranes contributed sand to the sequence through this time. Significantly, the
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tectonic setting evolved from the extensional rifting phase of the Pan African orogeny to a stable
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craton formed in the aftermath of the Neoproterozoic amalgamation of Gondwana and a passive
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continental shelf flanking the southern margin of the Paleo-Tethys, then the Meso-Tethys. In
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addition, the climate changed dramatically from hot humid through cold glacial, then back to
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warm humid. Furthermore, the depositional environment evolved from alluvial fans to proximal-
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distal braidplains, through shallow-deep marine, to sand flats or vast braidplains, to intertidal-
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offshore, and back to braided-meandering rivers.
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Mineral composition of parts of the siliciclastic sequence has been studied by several authors including Schneider et al. (1984, 2007), Khoury (1986), Weissbrod and Nachmias (1986), Amireh (1987, 1991, 1994), Amireh and Abed, 2000, and Amireh et al. (1994a, 2008).
Therefore, the present petrographic investigation aims at employing the uppermost
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Ediacaran-Lower Cretaceous siliciclastic sequence cropping out and sub-cropping in Jordan to
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assess the significance of each of the various factors governing the sandstone detrital framework
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modes. Furthermore, it attempts to answer the question whether plate tectonic setting is the
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primary factor influencing the sandstone‘s detrital light mineral composition.
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2. Geologic setting
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About 2500 meter-thick siliciclastic sequence with subordinate carbonates ranging in age from
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the late Ediacaran to the Late Cretaceous crops out and sub crops in certain parts of Jordan (Figs.
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2, 3). Its lower part constitutes a portion of the vast lower Paleozoic siliciclastic platform
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covering the outskirts of the East African orogen in northern Gondwana (Fig. 1, Peters, 1991)
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and blanketing the regional unconformity truncating the peripheral parts of the Arabian-Nubian
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Shield (Johnson et al., 2011, 2013). Fig. 1 demonstrates just discontinuous outcrops of the entire
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Paleozoic sequence, whereas the actual immense extension, particularly of the lower Paleozoic
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siliciclastic sheet covers completely the northern margin of Gondwana as revealed by the
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subsurface maps (Petters, 1991; Alsharhan and Nairn, 1997).
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The invoked siliciclastic system in Jordan consists of an uppermost Ediacaran series,
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lower Paleozoic succession (Cambrian and Ordovician Systems, and lower Silurian
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Series=Llandovery), and Lower Cretaceous Series.
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Uppermost Ediacaran Umm Ghaddah Formation rests non-conformably above upper
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Ediacaran Aheimir Volcanic Suite (Figs. 3, 4A, 5A), or Sarmuj Conglomerate (Fig. 5A) or
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Hayala Volcaniclastic Formations, and is unconformably overlain by Fortunian Salab Formation.
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It consists of a rhyolitic monomictic conglomerate facies (facies A) and a sandstone facies
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(facies B) deposited by an alluvial fan and a braided river flowing northeastward (Table 1, Figs.
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2, 5A), respectively, and characterized by a large-scale fining upward succession that reflects the
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gradual cessation of the Pan African orogeny (Amireh et al., 2008).
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The Fortunian Salab sandstone starts non-conformably above the Neoproterozoic
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metamorphic, intrusive, and extrusive basement of the Aqaba (Fig. 4B) and the Araba
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Complexes. Predominant sandstones, with much less abundant conglomerates and silt-mudstones
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constitute the fluvial lower Cambrian Salab and the overlying Cambrian Umm Ishrin Formations
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(Figs. 4C, D). Both formations received detritus through braided rives flowing northward from
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the southerly located Arabian Shield (Table 1, Figs. 2, 5B, C; Amireh et al., 1994b). The lower
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part of the latter formation is replaced north-westley by shallow marine, well-sorted sandstone of
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the Abu Khusheiba Formation, which, in turn, is replaced further north-westley by carbonates,
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sandstones and mudstones of the Burj Formation (Amireh et al., 1994b). Trilobites and
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brachiopods yielding the late early Cambrian age, and rare occurrences of interbedded
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volcaniclastic conglomerates and volcanic tuffs (Fig. 4F) characterize the latter formation. The
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Ordovician System is more marine-influenced and consists mainly of sandstones with minor silt-
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mudstones, but lacks the carbonates. Fluvial sandstones of the lower Disi Formation
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conformably overlie the Umm Ishrin clastics. The transport direction of the braided rivers is
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similar to that of the underlying fluvial formations, which is northward (Table 1, Figs. 2, 5C;
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Amireh et al., 2001). Four siltstone-fine sandstone units characterized by Cruziana species and
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other ichnofossils interrupt this fluvial sequence (Bender, 1968; Amireh et al., 2001). The second
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Umm Saham Formation, overlying the Disi Formation, consists of a sandy fluvial-dominated
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lower part having the same northward dispersal direction, (Table 1, Figs. 2, 5C; Amireh et al.,
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2001) and a finer clastic upper part deposited in an intertidal environment (Amireh, et al., 2001).
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A deeper marine environment replaced the intertidal conditions during deposition of the third
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overlying Hiswa Formation (Fig. 5D). It consists of lower fine sandstone with interbedded
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mudstones carrying graptolites and deposited in a deeper environment, the lower shoreface to
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offshore, that grades upwards into mid shelf storm deposits (Makhlouf, 1988) then into the
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shallower upper shoreface environment. The fourth Dubaydib Formation consists of fine to very
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fine sandstone facies alternating with siltstone facies, and was deposited within the upper to
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lower shoreface zone but affected by three storm events (Figs. 4E, 5D; Amireh, et al., 2001).
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Fluctuations between the upper-lower shoreface and the open marine offshore conditions
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persisted through deposition of the overlying Tubailiyat, Batra, and Ratya Members of the fifth
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Mudawwara Formation, as well as the conformably overlying Llandovery Khusha Formation
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(Fig. 5D). Various types of ichnofossils are pervasive throughout the last four marine formations.
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The remaining parts of the Silurian System as well as the Devonian and the
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Carboniferous Systems are missing from the stratigraphy of Jordan (Bender, 1968). Most
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probably, they were truncated through the Hercynian orogeny (Saint-Marc, 1978) that affected
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the region during the Carboniferous, as indicated by their presence in adjoining countries
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(Husseini, 1989, 2000).
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The Triassic and Jurassic Systems are mainly non-clastic deposits, thus are not studied.
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The Lower Cretaceous Kurnub Group in northern Jordan consists of the Ramel, the Jarash, and
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the Bir Fa‘as Formations composed mainly of fluvial sandstone, some siltstone and
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conglomerate with few interbedded shallow marine arenaceous dolostone-limestone units
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(Amireh, 1997; Amireh and Abed, 1999). In central and south Jordan, the Kurnub Group consists
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of the Karak and Hammamat Formations composed entirely of terrestrial sandstone, and
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overlying the Bir Fa‘as Formation consisting of shallow marine sandstone and carbonate
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(Amireh, 2000). The transport direction of the braided to low sinuosity meandering rivers is
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persistently from the south-located Arabian Shield provenance towards the north and northwest-
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located Neo-Tethys (Table 1, Figs. 2, 5E; Amireh, 1993: 1997; 2000, Amireh and Abed, 1999).
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The Upper Cretaceous Series is composed of carbonates, evaporites, cherts, oil shales and
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phosphorites of the Ajlun and the Belqa Groups (Fig. 3).
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3. Tectonic and depositional environment development
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The uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan, the lower part of
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which constitutes a segment of the immense lower Paleozoic siliciclastic sheet blanketing most
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of the northern Gondwana margin and extending now from Arabia westward across north Africa
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to northwest and west Africa (Fig. 1, Peters, 1991). The Jordanian lower Paleozoic siliciclastic
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sequence received detrital sediment influx constantly from the Arabian-Nubian Shield, whereas
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the Mesozoic sequence received detritus additionally from the Paleozoic platform strata. The
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transport direction through braided rivers persisted from the south-located provenance towards
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the north and northwest located-Paleo and Neo-Tethys (Fig. 2). Following is a summary of
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tectonic events involved in the genesis of the Arabian Shield, and the depositional environment
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development of these platform strata, which are partly demonstrated in Fig. 5 as a series of five
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tectono sedimentary block diagrams.
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From the Mesoproterozoic (ca 1200 Ma) until ca 950 Ma the Mozambique Ocean opened
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by rifting of the eastern margin of the African Craton, within the Rodinia supercontinent. This
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rifting was associated with sea floor spreading (Hoffman, 1999). Several continental microplates
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and island arcs were produced then collided and accreted during the time interval of ca 950–750
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Ma forming the Arabian Shield (Stoeser and Camp, 1985; Al Shanti, 2009). Later on, the
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western part of the Arabian Shield collided with the African NE margin of Gondwana
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(Abdelsalam and Stern, 1996), closing the Mozambique Ocean and being welded to the northern
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part of the East African orogen (Hoffman, 1999), particularly the Saharan Metacraton (Fig. 1,
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Johnson et al., 2011). This thermo-tectonic activity is termed the Pan African orogeny (Kröner,
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1984). Afterwards, the western margin of the Arabian Shield collided with its central and eastern
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parts, thus suturing the Arabian Shield with the African Continent between 640 and 620 Ma
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(Husseini, 2000). This cratonization phase of accretionary and collisional (compressional)
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tectonic processes and the complete assembly of the Arabian Shield gave rise to a new (Proto)
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Arabian Craton (Al Shanti, 2009). An extensional collapse phase accompanied by deposition in
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syn-rift basins replaced the compressional phase during the time interval between 630 and 530
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Ma (Husseini, 1989, 2000; Abdelsalam and Stern, 1996). Intrusions of postorogenic alkali rich
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granites and rhyolites (Jarrar et al., 2008) dominated this extensional phase. The extensional
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collapse of the Proto Arabian Craton witnessed the development of the regionally extensive Najd
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Fault System and its complimentary syn-rift, down block-faulted, extensional basins (Fig. 5A)
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with associated alkali rich granites and rhyolites (Jarrar, et al., 2003; Powell et al., 2015). The
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Najd faults were active between about 630 Ma and 555 Ma (Johnson and Kattan, 2012), and
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ceased gradually after that to end completely at about 530 Ma, prior to deposition of the
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Cambrian sandstones over a vast peneplain situated at the eastern, northern, and northwestern
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edge of the Arabian Shield (Johnson, et al., 2011).
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Following the extensional rifting phase, which terminates the Neoproterozoic
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amalgamation of northern Gondwana, an isostatic uplift and the accompanying erosion of the
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Neoproterozoic Aqaba Complex (Arabian Shield) and the later, but more localized, Ediacaran
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Araba Complex cropping out in Wadi Araba (Fig. 2) took place. This extensive erosional phase
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of the Jordanian basement complex gave rise to a peneplain, called Rum Unconformity (Fig. 4B;
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Powell et al., 2014). The latter constitutes a fraction of the regional unconformity truncating the
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peripheral parts of the Arabian-Nubian Shield (Johnson et al., 2011, 2013). Terrestrial
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sedimentation had overlain this unconformity surface during the early Cambrian (Fig. 5B). A
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regional transgression of the Paleo-Tethys affected Jordan in the late early to mid-Cambrian that
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was responsible for deposition of the regional Burj carbonates (Amireh et al., 1994b; Powell et
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al., 2014) and followed by regressive siliciclastics. Terrestrial conditions resumed through the
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remaining part of the Cambrian and through the Early Ordovician (Fig. 5C). Subsequently,
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shallow marine conditions dominated the study area during the Middle and Late Ordovician as
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being a stable subsiding shelf along the northeastern margin of Gondwana (Fig. 5D)
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(McGillivray and Husseini, 1992). At the end of the Late Ordovician, polar glaciers expanded
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across Gondwana and covered most of western Arabia, including Jordan (Abed et. al, 1993), as
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well as North Africa (Beuf et al., 1966). In the early Silurian, the retreat of glaciers introduced an
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abrupt sea level rise and deposition of marginal marine shales that covered most of Gondwana
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shelf. Therefore, Jordan was part of the stable Arabian Craton at the northeastern passive margin
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of Gondwana facing the southern margin of the Paleo-Tethys during the early to mid-Paleozoic.
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Moreover, no orogenies are recorded in Jordan from the mid Cambrian to the late Devonian.
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In the late Carboniferous, a thermo-tectonic orogeny caused a regional domal uplift;
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called “Geanticline of Heletz” (Gvirtzman and Weissbrod, 1984) affected Jordan and extended
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from Sinai north to the western Palmyrides. This regional uplift is probably a manifestation of
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the Hercynian (or Variscan) orogeny that was caused by collision and welding of Gondwana
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with Laurassia leading to assembly of the supercontinent Pangaea during the late Carboniferous.
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The uplift was associated with rifting and magmatism and subjected to extensive erosion leading
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to a significant hiatus in Jordan stripping away the Ordovician through the Devonian especially
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in western Jordan, and giving rise to a NS strip-like configuration of the Cambrian and the
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Ordovician outcrops in Jordan (Fig. 2).
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In the late Permian and Triassic, the Turkish and Sanadaj-Sirjan area of the Cimmerian
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Continent became separated from the Arabian Gondwana by the Zagros rift initiating the Neo-
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Tethys (Şengör et al., 1988). During the Triassic (to Early Jurassic), an extensional phase
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resulted due to continued rifting along the Zagros suture (Şengör et al., 1988) that extended and
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stretched the Arabian plate, causing deep-seated normal faults. From the Early to the Late
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Jurassic Arabia again entered a period of tectonic quiescence.
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At the close up of the Jurassic, the lithospheric extension, continental rifting, and
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associated uplift resumed in Arabia due to continuation of the breakup processes in Gondwana
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(Guiraud and Maurin, 1992). The orogenic uplift of the block faulted continental crust was
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accompanied by a deep erosional phase that truncated a great proportion of the Jurassic sequence
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in Jordan (Bender, 1968; Bandel, 1981). This extensive erosion is indicated by presence of a
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basal conglomerate lining the unconformity surface above the remaining Middle Jurassic
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sequence (Amireh, 1997; Amireh and Abed, 1999). Gradually, and through the Early Cretaceous,
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the tectonic uplift ceased in the region, and tectonic quiescence prevailed. Consequently, fluvial
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sedimentation dominated in central and southern Jordan (Fig. 5E), whereas northern Jordan,
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which is closer to the Neo-Tethys, was affected by several marine ingressions (Amireh, 1997;
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Amireh and Abed, 1999). During the Late Cretaceous, Jordan within Arabia was widely
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transgressed by the Neo-Tethys (Dercourt et al., 1993).
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4. Arabian-Nubian Shield provenance
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The paleocurrent directions determined through 1339 reliable measurements of planar
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and trough cross bedding azimuths in the uppermost Ediacaran-Lower Cretaceous siliciclastic
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sequence are summarized in Table 1 following Amireh (1993, 1997, 2000), Amireh and Abed
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(1999), and Amireh et al. (1994b, 2001, 2008). In addition, these paleocurrents are portrayed on
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the geological map of Jordan (Fig. 2), and demonstrated by the tectono sedimentary block
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diagrams (Fig. 5). According to these paleocurrent dispersal directions, the southerly-located
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Arabian-Nubian Shield (ANS) can be determined with a great significance to represent the
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constant provenance for the siliciclastic sequence in Jordan throughout the late Ediacaran-Late
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Cretaceous. In the Paleozoic Era, the detritus was shed from this southerly ANS provenance and
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transported by braided rivers towards the north and northwest-located Paleo-Tethys (Bender,
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1968; Schneider et al., 1984, 2007; Amireh, 1987, 1991, 1992, 1993; Amireh et al., 1994b, 2001;
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Powell, 1989). In the Mesozoic Era, braided and low sinuosity meandering rivers, similarly,
274
transported siliciclastic sediments from this southerly ANS to the north and northwest-located
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Neo-Tethys (Bender, 1968; Amireh, 1987, 1991, 1993, 1997, 2000; Amireh and Abed, 1999).
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This northward dispersal direction from the southerly ANS towards the north and northwest-
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located Paleo then Neo-Tethys during the Paleozoic and Mesozoic, respectively, is also well-
278
recorded in the adjacent countries (Weissbrod and Nachmias, 1986; Klitzsch and Squyres, 1990;
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Alsharahn and Nairn, 1997; Garfunkle, 1999, 2002).
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Moreover, this ANS provenance is recently confirmed through SHRIMP and SIMS U-Pb
281
geochronological dating of detrital zircon grains from these siliciclastic deposits (Kröner et al.,
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1990, Stern et al., 1994; Wilde and Youssef, 2002; Avigad et al., 2003, 2015; Kolodner et al.,
283
2006; Samuel and Youssef, 2011; Morag et al., 2012; Yaseen et al. 2013; and Nasiri Bezenjani,
284
et al., 2014).
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Yaseen et al. (2013) constrained ages ranging between 650 and 600 Ma in the Saramuj
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Conglomerate Formation constituting part of the basement below the sequence under
287
investigation (Figs. 1, 2), and recorded the ANS to be the provenance, particularly the Aqaba
288
Complex now exposed in southern Jordan within the northernmost part of the ANS. Just west of
289
the study area, Kröner et al. (1990), Avigad et al. (2003, 2015, 2017), Kolodner et al. (2006), and
290
Morag et al. (2012) similarly recorded this Neoproterozoic ANS provenance for the Cambrian
291
and Ordovician siliciclastic sequence. Kröner et al. (1990) dated detrital zircon grains from
292
several rock types in Elat basement and in the adjacent Sinai (Fig. 1) to range from 820 to 800
293
Ma.
294
Avigad, et al. (2003) recorded a 550-650 Ma age of detrital zircon grains in Cambrian
295
unit in Elat area (Fig. 1) that indicates the calk alkaline and alkaline igneous rocks of the
296
Neoproterozoic ANS provenance. They documented, also, zircon grains yielding older ages, pre
297
Neoproterozoic that reach up to 2.7 Ga, which may indicate the Saharan Metacraton provenance,
298
or the southern Affif terrane in northwest Arabia (Fig. 1). Avigad et al. (2015) based on U-Pb-Hf
299
detrital zircon geochronology of the Zenifim Formation subcropping in Northern and Southern
300
Negev (Fig. 1) identified the granites of the adjacent ANS formed at the cessation of the
301
Neoproterozoic orogeny as a major provenance for these late Ediacaran arkoses.
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Recently, Avigad et al. (2017) used detrital rutile U-Pb geochronology to deduce a broad North
303
African source for the Cambro-Ordovician sandstone cropping out in Elat area (Fig. 1), southern
304
Jordan, and Ethiopia.
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Kolodner et al. (2006) constrained a U-Pb (900-530 Ma) age indicating derivation of the
306
Cambrian and Ordovician siliciclastics from the proximal northern part of the Arabian-Nubian
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Shield. They attributed older ages that reach up to 2.7 Ga, to be derived from a more distal
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southern provenance, such as the northern parts of the Tanzanian-Congo (Fig. 1) and the
309
Dhrawer Cratons, or a western provenance such as the Western Desert, or the Gebel Oweinat
310
area (Fig. 1). Kolodner et al. (2009) also investigated the detrital zircon U-Pb in Lower
311
Cretaceous sandstone cropping out in Northern Negev (Fig. 1), and Elat region (Fig. 1), and
312
concluded that they are mostly derived from reworking of the Paleozoic section. Morag et al.
313
(2012) documented a northern ANS as a provenance to the Elat conglomerate unit (Fig. 1) based
314
on detrital zircon grains ranging in age from 1.0 Ga to around 580 Ma.
315
Westward, at southern Sinai (Fig. 1), Samuel et al. (2011) constrained the age of the
316
Rutig conglomerate between 850 and 600 Ma, concluded the provenance to be the ANS material
317
in Sinai, and confined deposition of different levels of the conglomerates to ca 620–610 Ma and
318
600–590 Ma.
319
Farther westward, Wilde and Youssef (2002) constrained the age of the sedimentary
320
Hammamat Group in the North Eastern Desert (Fig. 1), to be 585 ± 13 Ma, and concluded that
321
the zircon grains were derived from the adjacent Dokhan Volcanic Series. In addition, they
322
recorded older ages, up to ca 2630 Ma, indicating contributions from Proterozoic and Archean
323
sources that may lie in the Central and South Eastern Desert (Fig. 1), the Nile Craton, or in a
324
remote part of the ANS.
17
325
Southwestward of study area, Stern et al. (1994) dated conglomerates and other
326
metamorphic and igneous rocks of the Precambrian basement around Wadi Halfa (Fig. 1), to
327
range from 2.6 to 0.72 Ga, and concluded that the conglomerate is derived from a local source.
328 329
Southward of study area, the age of Talbah Group in the Midyan terrane of NW Arabia
330
(Fig. 1) is constrained by Nasiri Bezenjani, et al. (2014) to range from 635 ± 5 Ma to 569 ± 10
331
Ma. They recorded also that it derived detritus from the Central Eastern Desert and Midyan
332
terrane island arc basement for its lower and middle parts, and from other parts of the ANS for
333
its upper part. In the same region, detrital zircon grains from tuff beds in the Dhaiqa and Rubtayn
334
basins within the Jibalah Group (Fig. 1) yields SIMS U-Pb ages suggesting deposition between
335
600 and 570 Ma (Kennedy et al., 2011).
336
337
5. Methods and terminology
338
The bulk petrographic compositional approach is applied in the present study. Three hundred
339
forty one fresh siliciclastic sandstone samples were collected from 19 profiles across the
340
outcrops of the uppermost Ediacaran-Lower Cretaceous clastic sequence, and from oil
341
exploration wells HM-2, AJ-1, NH-1, and WS-3 in Jordan (Fig. 2). The outcrop and well-core
342
sandstones are mainly medium to coarse-grained leading to reliable identification and favorable
343
counting results. The sandstone samples were thin-sectioned after epoxy impregnation for the
344
semi indurate or slightly friable samples. Subsequently, they were examined by the routine
345
polarized light microscope. About 500 points were counted in each thin section to determine the
18
346
modes of the detrital framework grains, the detrital matrix and the cements. Counting errors for
347
the grain parameters are less than 5% of the whole rock for individual counts.
348
Gazzi-Dickinson point counting method (Ingersoll et al., 1984) that minimizes the
349
dependence of composition on grain size is employed to achieve reliable results (Gazzi, 1966;
350
Dickinson, 1970; Ingersoll, 2012). Moreover, all sandstone samples employed for point counting
351
have intact framework grains not affected by diagenesis, particularly intrastratal solution and
352
replacement as indicated by having a matrix and/or a cement generally not exceeding 25% that
353
would otherwise both affect or alter the framework constituents (cf. Dickinson and Suczek,
354
1979; Dickinson et al., 1983). Additionally, the matrix and the cements just fill passively the
355
interstitial spaces between the framework grains, not altering them, and thus leading to reliable
356
identification.
357
The framework modes of quartz, feldspar and lithic fragments are recalculated to 100%
358
in order to determine the type of the sandstone applying a modified classification of Pettijohn et
359
al. (1987; Fig. 6). The modifications represent an addition of a prefix to the class of the
360
sandstone expressing a characteristic component not appearing in the classification, and
361
subdivision of the arkose field into arkosic arenite and lithic arkosic arenite subfields, as well as
362
subdivision of the lithic arenite field into feldspathic litharenite and litharenite subfields.
363
The variants of quartz, feldspar, and lithic fragments are recalculated to the various
364
petrographic parameters to be plotted in the triangular compositional diagrams of Dickinson and
365
Suczek (1979) and Dickinson et al. (1983).
19
366
367
6. Results
368
The mean, standard deviation, and confidence level of 95% for the sandstone component
369
parameters obtained for each member, formation, or group are listed in Table 2 and Appendix A.
370
The means of the framework modes for most of the formations have standard deviations
371
(STDEV. S) less than 10%, and rarely 10 to 15% of the whole rock (Table 2). Such values of
372
standard deviations of means imply that the formations are petrographically homogenous. The
373
“P” values of confidence level 95% calculated for the formations (Table 2; Appendix A),
374
excluding the null hypothesis value or empty set having no elements in the set, are mainly less
375
than the significance (alpha) level of 0.05, thus indicating the statistical significance of the
376
various component parameters (hypothesis test).
377
The sandstone components parameters include the modes of: framework grains (FW,
378
Figs. 7-9), detrital matrix (Mt, Fig. 7A), cements (C, Figs. 7B-E), total quartz (Qt), total feldspar
379
(F), lithic fragments (L), monocrystalline quartz (Qm), polycrystalline quartz (Qp), total lithic
380
fragments (Lt), volcanic lithic fragments (Lv), sedimentary/metasedimentary lithic fragments
381
(Ls), plagioclase (P), and K-feldspar (K).
382
Qt equals the sum of Qm (Figs. 7B, D, E, F) and Qp (Figs. 8A, B), whereas F represents
383
the sum of K-feldspar (mainly orthoclase, Fig. 8E, and less commonly microcline, Fig. 8F) and
384
plagioclase. L equals the sum of Lv (Figs. 8C, D, 9A-E) and Ls (Figs. 10A-D), whereas Lt
385
represents the sum of L and Qp.
20
386
Triangular QtFL, QmFLt, QpLvLs, and QmPK compositional diagrams following
387
Dickinson and Suczek (1979) and Dickinson et al. (1983) are constructed for the mean
388
framework modes for all the members, formations, or groups of the investigated sequence (Fig.
389
11). Moreover, representation of all individual samples on these compositional diagrams is
390
available at the link: http://link-placeholder.com .
391
Based upon the total quartz (Qt), total feldspar (F) and lithic fragments (L) parameters for the
392
members, formations or groups investigated, the types of sandstone are determined applying the
393
modified classification of Pettijhon et al., (1987) (Fig. 6).
394
395
7. Discussion
396
The uppermost Ediacaran-Lower Cretaceous clastic sequence under investigation can be split
397
into five sandstone suites. Each one consists of a group of sandstone samples that are closely
398
related both spatially and stratigraphically (cf., Dickinson et al., 1983) and having same
399
sandstone type. The individual sandstone suite represents either one formation or several
400
associated formations, for each of which the common framework modes, might indicate
401
derivation from a specific provenance terrane, thus represents mainly, a relatively unchanged
402
plate tectonic setting. However, interpretation of the detrital framework modes is based upon the
403
individual formations rather than the sandstone suites. From other point of view, this
404
interpretation of modal composition is based upon comparison with present-day plate tectonic
405
processes that probably were different during the Paleozoic and Mesozoic, and particularly
21
406
during the late Ediacaran. However, Dickinson‘s plate tectonic provenance approach is
407
established mainly upon Paleozoic and Mesozoic, and some late Precambrian sandstone suites
408
(sandstone suites numbers 10, 11 and 25, Dickinson and Suczek, 1979; latest Precambrian to mid
409
Ordovician sandstone suite, Dickinson, et al., 1983).
410
411
7.1. Sandstone suite number 1: Umm Ghaddah Formation of late Ediacaran-early Cambrian age
412
Umm Ghaddah Formation consists of a conglomerate facies and a sandstone facies. The detrital
413
framework modes of the sandy matrix of the conglomerates and the sandstones is composed
414
mainly of monocrystalline and polycrystalline quartz, K-feldspar, rhyolitic rock fragments,
415
subordinate plagioclase and rare sedimentary and metamorphic lithic fragments (Table 2).
416
According to the means of the Qt, F, and R (L) parameters (Table 2), the sandstone is classified
417
as a rhyolitic litharenite (Fig. 6).
418
It can be seen from the QtFL compositional diagram (Fig. 11A) that the means of these
419
parameters fall within the recycled orogenic provenance field. The QmFLt plot (Fig. 11B)
420
augments this inference, and specifies it to be the transitional recycled orogenic provenance.
421
According to the QpLvLs and QmPK compositional diagrams (Figs. 11C, D), the provenance
422
terrane can be inferred to be the magmatic arc orogen, and the continental block or the recycled
423
orogenic terrane, respectively. Which one of these inferences is true? An attempt to answer this
424
question will follow integrating the achieved petrographic results, together with the tectonic,
22
425
geologic, sedimentological, and climatological data presented in the section of tectonic and
426
depositional environment development.
427
Umm Ghaddah Formation has an age ranging from the late Ediacaran to the early
428
Cambrian (Amireh, et al., 2008). This age could be constrained between 598.2 ± 3.8 Ma, the age
429
of the underlying Aheimir Volcanic Suite (Jarrar et al., 2012), and tentatively 541 Ma (Fortunian
430
Age, Cohen et al., 2016), the age of the overlying Salab Formation dated by Amireh et al.
431
(1994b) according to the presence of Cruziana aegyptica ichnofossil. At this time span, the
432
Arabian Shield provenance has already been stabilized or cratonized into the stable craton “Proto
433
Arabian Craton” devoid of collisional-accretional magmatic arcs processes that ceased at about
434
630 Ma (Al Shanti, 2009), thus before deposition of the present formation.
435
Moreover, the magmatic arc provenance terrane can be refuted according to the following
436
petrographic criteria. 1) The rarity of plagioclase (Table 2), since the sands derived from most
437
magmatic arcs are commonly enriched with plagioclase or, are characterized by a high ratio of
438
plagioclase to K-feldspar (Dickinson 1985; Ingersoll, 2012). 2) The quartz content is higher here
439
than that of typical magmatic arc terranes (Dickinson and Suczek, 1979). 3) The types of the
440
lithic fragments being mainly acidic rhyolitic (Figs. 8C, D, 9A-E) rather than intermediate
441
andesitic or basic basaltic (Fig. 9F) as the sands derived from most magmatic arcs of
442
intermediate-composition (Dickinson, 1985; Marsaglia and Ingersoll, 1992; Ingersoll, 2012).
443
These rhyolitic lithic fragments were derived mainly from a local provenance; upper Ediacaran
444
Aheimir Volcanic Suite, cropping out in central part of Wadi Araba (Fig. 2), and not related
23
445
genetically to any island arc but represents an intracratonic syn-rift volcanic extrusion (Jarrar,
446
1992; Jarrar et al., 1992).
447
Regarding the inferred recycled orogenic provenance, the subduction complexes of
448
deformed oceanic sediments and lavas can be excluded based on the absence or rarity of clasts
449
indicating shedding from ophiolites and oceanic crust, or from other sedimentary source, such as
450
greenstone, chert (Figs. 8C, D, 8A, E), shale, argillite, slate, phyllite, greywacke and limestone
451
(Dickinson and Suczek , 1979; Dickinson, 1985). The recycled collisional orogenic and the
452
foreland uplifts associated with foreland fold thrust belts provenance types can be also ruled out
453
according to the rarity of sedimentary (Figs. 10A, B) and metasedimentary lithic fragments (Figs.
454
10C, D), and absence of criteria indicative of recycling, such as two stages of syntaxial quartz
455
overgrowths.
456
This erroneous magmatic arc and recycled orogenic provenance terranes interpretation
457
employing Dickinson‘s petrographic model might be attributed to the high mode of the rhyolitic
458
lithic fragments (Table 2). They were contributed from the local, post-orogenic Aheimir
459
intracratonic syn-rift extrusion, where the plate tectonic setting of these rift-related volcanic
460
rocks are not represented by Dickinson‘s Plate tectonics-provenance diagrams. They cause
461
pulling of the means of the QtFL, QmFLt parameters to fall in the erroneous recycled orogenic,
462
and transitional recycled orogenic provenance fields, respectively, departing probably from the
463
more appropriate basement uplift continental block field. Furthermore, they also cause the means
464
of the QpLvLs parameters to fall erroneously close to the Lv pole in the magmatic arc
465
provenance field. Consequently, in order to interpret the detrital framework modes, the proposed
24
466
provenance terrane, as well as the other sedimentological and climatological factors should be
467
evaluated.
468
At the late Ediacaran-early Cambrian the study area underwent the final extensional
469
rifting phase of the Pan African orogeny (Jarrar et al., 1991) that caused block faulting of the
470
Arabian Shield leading to development of a series of half-grabens, grabens and horsts, or
471
generally local uplifted basement blocks (Fig. 5A). Therefore, a basement uplift provenance
472
terrane of the NE Gondwana continental block seems to be the most appropriate one. Amireh et
473
al. (2008) recorded that Umm Ghaddah Formation was deposited in intracratonic rift system
474
basins bounded by active listric half-graben faults (Fig. 5A). Their uplifted shoulders,
475
particularly the footwall upland, and the hangingwall lowland source rocks, as well as the
476
intrabasinal horst structures were subjected to a high rate of erosion. Consequently, coarse
477
gravelly detritus was shed and rapidly deposited in the intracratonic basins as transverse alluvial
478
fans, whereas the sandy debris was deposited as a proximal axial braidplain (Fig. 5A). The
479
source rocks were the granitoids and gneisses of the Aqaba and the Araba Complexes of the
480
Arabian Shield, and the local Aheimir Volcanic Suite (Figs. 2, 5A). The latter source rocks
481
contributed the gravely debris to the adjacent intermontane rift basins as those depicted in
482
profiles number 12 and 13 (Fig. 2; Amireh et al., 2008), and the sand to the further rift basins as
483
those represented in profile number 16 and in HM-2, WS-3, AJ-1, and NH-3 wells (Fig. 2;
484
Amireh et al., 2008). On the other hand, the monocrystalline and polycrystalline quartz, K-
485
feldspar, and plagioclase grains were delivered to all the intermontane rift basins from the
486
Arabian Shield, where its northern flank crops out in southwestern Jordan (Fig. 2), as discussed
487
in section 3.
25
488
The source rocks and the released detritus were subjected to an intense chemical
489
weathering due to the prevailing hot humid climate (Wolfart, 1981, Konert et al., 2001, Amireh
490
et al., 2008). Under these conditions of active tectonic uplift, high relief, high rate of erosion,
491
very short transport distance, and rapid sedimentation in proximal alluvial fans and braidplains
492
within the adjacent intermontane rift basins, a great proportion of the rhyolitic lithic fragments
493
(L= 44.4%, mainly Lv, Table 2) could escape the intense chemical weathering. On the other
494
hand, through the longer transport distance of the sandy detritus from the Aqaba and the Araba
495
Complexes, and probably from other southern parts of the Arabian Shield, to the depositional
496
intermontane rift basins (Fig. 2), the intense chemical weathering as well as the mechanical
497
weathering could dissolve and destruct a large proportion of the unstable feldspars. The survived
498
remnants, mainly K-feldspar and rarely plagioclase (F= 12.6%, Table 2), together with the stable
499
quartz varieties (Qt= 43.0%), and the rhyolitic lithic fragments managed to arrive safely to the
500
depositional intermontane rift basins, and to give rise ultimately to the immature rhyolitic
501
litharenites.
502
503
7.2. Sandstone suite number 2: Salab, Burj and Abu Khusheiba Formations of early to mid-
504
Cambrian age
505
Sandstone suite number 2 consists of the lower Cambrian Salab, the overlying lower-middle
506
Cambrian Burj, and the coeval Abu Khusheiba Formations. The Salab Formation has a
507
subarkosic arenite composition (F= 17.2%, Table 2; Figs. 8E, F) and the Abu Khusheiba
508
Formation is also composed of subarkosic arenite but with a lower feldspar mode (F=11%, Table
26
509
2). On the other hand, the Burj Formation has a rhyolitic sublitharenite composition (F= 7.5%,
510
L= 20%, Table 2).
511
It can be seen from QtFL compositional diagram (Fig. 11A) that the means of these
512
parameters for the Salab, Abu Khusheiba, and Burj Formations fall in the transitional continental
513
block, craton interior continental block, and recycled orogenic provenance terranes, respectively.
514
The QmFLt plot (Fig. 11B) augments the inference for the Salab and Abu Khusheiba
515
Formations, and specifies the provenance terrane for the Burj Formation to be the quartzose
516
recycled orogen. Upon employing the QpLvLs compositional diagram (Fig. 11C); the means of
517
these parameters for the Burj Formation fall in the mixed orogenic provenance terrane
518
contradicting with those derived from the QtFL and QmFLt plots. On the other hand, plotting
519
means of the QmPK parameters for the three formations (Fig. 11D) yields a better result, where
520
all of them are located close to the Qm pole indicating an increasing maturity or stability of
521
detritus derived from the continental block provenance terranes (Dickinson and Suczek, 1979).
522
In contrast to the Lv parameter, the P, and K parameters of the three formations are both
523
petrographically homogenous and statistically significant (Table 2).
524
The transitional continental block and the craton interior continental block provenance
525
terranes inferred for the Salab and the Abu Khusheiba Formations, respectively, fit very well
526
with the petrographic and the other data documented here. Therefore, the modal framework
527
composition of both formations can be fully interpreted based upon these inferred provenance
528
terranes together with the influence of the other secondary factors.
27
529
The last extensional rifting phase of the Pan African orogeny started to cease gradually
530
from the late Ediacaran (cf. Husseini, 1989; Abdelsalam and Stern, 1996; Jarrar et al., 2003;
531
Amireh et al., 2008), so that at the early Cambrian, a much-reduced tectonic uplift prevailed, less
532
than that of Umm Ghaddah Formation. Consequently, the continental block was less affected by
533
the block faulting processes leading to a reduced basement uplift. The plate tectonic setting of
534
the continental block corresponds most probably to the transitional provenance terrane.
535
Therefore, a moderate relief characterized the Arabian Shield source rocks; intermediate between
536
the high relief of the basement uplifts and the low relief of the craton interior. This moderate
537
relief also characterized the rhyolite paleohigh that existed in Wadi Abu Khusheiba area, central
538
Wadi Araba (Abed, 2000), which was probably a broad positive topography rather than a strong
539
local relief as those produced by the block-faulting phase of the Pan Africa orogeny and
540
characterized the Umm Ghaddah Formation. This moderate relief was in turn responsible for a
541
moderate rate of erosion. Under the persisting hot humid climate, the intensive chemical
542
weathering continued affecting the granitoids and the gneissic source rocks and the sandy
543
detritus consisting of unstable feldspars and rhyolitic lithic fragments, and the stable quartz
544
varieties. However, the sediments were transported relatively a short distance by braided rivers,
545
and rapidly deposited in sand flats of the proximal-medial braidplains (Profiles number 1 and 14,
546
Fig. 2; Amireh et al., 1994b). Such conditions gave a chance to a great proportion of the unstable
547
feldspar grains (F= 17.2%, Table 2) to escape the intense chemical weathering and the
548
mechanical weathering during transit, and to reach the fluvial depositional environment. These
549
feldspars together with the stable quartz gave rise ultimately to the immature subarkosic arenites
550
of the Salab Formation.
28
551
The lower mode of feldspars of the overlying Abu Khusheiba Formation (F= 11.0%,
552
Table 2) can be attributed to the lower relief of the inferred craton interior provenance terrane
553
due to the almost complete cease of the Pan African orogeny. Consequently, the low relief
554
contributed feldspar grains at a retarded rate of erosion, which were severely affected by the
555
prevailing chemical weathering. Moreover, the feldspars were also partially destructed by the
556
mechanical attrition in the more energetic beach depositional environment of the Abu Khusheiba
557
Formation (Amireh, 1987; Amireh et al., 1994b).
558
The inferred quartzose recycled orogenic provenance terrane of the Burj Formation
559
seems to be erroneous according to the absence of the petrographic evidence indicating
560
reworking from the stratal source rocks, such as a high mode of sedimentary or metamorphic
561
lithic clasts, where Ls attains only 4.1% (Table 2), or presence of two stages of quartz
562
overgrowths. Additionally, no folded strata or thrust belts are recorded in the Arabian Craton
563
source rocks as discussed in the tectonic and depositional environment development section.
564
Moreover, the high modes of the rhyolitic lithic fragments (L= 22.0%, Lv= 61.9%, Table 2)
565
derived from the local sources cause pulling of the means of the QmFL parameters to fall in the
566
quartzose recycled orogenic provenance subfield departing from the more appropriate craton
567
interior provenance terrane of the continental block. Additionally, the latter provenance terrane is
568
implied upon comparison with that of the covalent Abu Khusheiba Formation, where almost
569
similar conditions prevailed. However, the higher rhyolitic lithic fragments mode in the Burj
570
Formation could be attributed to the influence of a nearby local rhyolitic extrusion, located
571
north-westley of Wadi Araba (Fig. 2), and formed during the last postorogenic volcanism of the
29
572
extensional rifting phase of the Pan African orogeny that might lasted sometime in the Cambrian
573
(Beyth and Heimann, 1999).
574
This volcanic activity, which was blanketed by the succeeding fluvial siliciclastics of
575
Umm Ishrin Formation, is rather different from the older, more voluminous Neoproterozoic
576
Aheimir Volcanic suite that configured paleohighs at time of deposition of the Abu Khusheiba
577
Formation, and the coeval Burj Formation. Position of this postulated volcanic extrusion is
578
indicated here from the systematic southeastward decrease of the rhyolitic lithic fragments
579
modes in the three lateral covalent Burj, Abu Khusheiba, and the lower part of the Umm Ishrin
580
Formation, where they attain 22.0%, 1.8%, and 0.3%, respectively (Table 2). Figure 4F shows a
581
volcaniclastic conglomerate bed and a volcanic ash layer, among others recorded by Amireh
582
(1987), interbedded in the Burj Formation that could also indicate such volcanic source.
583
According to these volcaniclastic conglomerate and the volcanic ash layer Amireh (1987, p. 13)
584
recorded the presence of a “nearby volcanic activity”.
585
From other point of view, it should be stated here, that this proposed volcanic activity
586
delivered volcanic detritus to the depositional site with a variable rate through the time of the
587
Burj Formation, where Lv mode ranges from 0 to 63 (Appendix A.3). This variable rate of
588
volcanic flux is responsible for the high standard deviation of the Lv parameter recorded in the
589
Burj Formation that attains 31.6% (Table 2, Appendix A.3).
590
Moreover, the presence of devitrified volcaniclasts exhibiting original glassy textures, and
591
devitrified feldspar and pyroclastic phenocrysts (Figs. 9C, D) might substantiate the existence of
592
this volcanic activity. Additionally, the occurrence of barite cement (Amireh, 1987, 1991), and
30
593
apatite overgrowth (Fig. 8F), which are diagenetic processes indicative of volcanic-hydrothermal
594
activities (Bentz and Martini, 1968; Ramdohr, 1975) could further confirm the invoked volcanic
595
activity. It can be argued, that the apatite overgrowth results from the lower-middle Cambrian
596
major worldwide episode of phosphorite formation (Brasier and Callow, 2007). This argument
597
can be disregarded since this apatite overgrowth occurs in the lower part of the fluvial Umm
598
Ishrin Formation, which surely was not affected by this marine phosphorite depositional event.
599
600
7.3. Sandstone suite number 3: Umm Ishrin, Disi and Umm Saham Formations of mid-
601
Cambrian to Mid-Ordovician age
602
Sandstone suite number 3 consists of the middle-upper Cambrian Umm Ishrin, the upper
603
Cambrian-Lower Ordovician Disi, and the Lower Ordovician Umm Saham Formations that were
604
deposited by braided rivers on the southern stable shelf of the Paleo-Tethys flanking the Arabian
605
Shield. This sandstone suite is composed entirely of super mature quartzarenites (Fig. 6) devoid
606
of any single feldspar grain. Invariably, the QtFL compositional diagram (Fig. 11A) exhibits the
607
craton interior of the continental block as the sole provenance terrane for the three formations.
608
Additionally, the QmFLt compositional diagram (Fig. 11B) augments this result for the Umm
609
Saham Formation, and displays the Umm Ishrin and the Disi Formations to fall at the boundary
610
between the craton interior and the quartzose recycled orogenic provenance subfields. The
611
QpLvLs and QmPK compositional diagrams (Figs. 11C, D) have no significance, since the
612
modes of these parameters for the three formations are either zero or very low (Table 2). This is
613
normally the case for the craton interior sandstone suites (Dickinson and Suczek, 1979).
31
614
The inferred craton interior provenance terrane of the continental block fits very well
615
with the achieved petrographic data and observations. However, the influence of the other factors
616
should be also assessed. The granitoids and gneisses of the Arabian Shield consistently supplied
617
sandy detritus to the present sandstone suite in a similar way to the previous ones. The
618
siliciclastic debris included the two varieties of quartz, feldspars, and rhyolitic rock fragments.
619
At the mid-Cambrian to Mid-Ordovician time, no orogenic activity has been recorded in the
620
study area. Consequently, the source rocks were characterized by a broad positive low relief
621
leading to a retarded rate of erosion. Intense chemical weathering under the persisting warm
622
humid climate affected the source rocks with the low gradients, as well as the slowly released
623
sandy detritus that were further transported a long distance by braided rivers across continental
624
surfaces having low gradients to the distal braidplains (Amireh et al., 1994b; Amireh et al.,
625
2001). The sediments that resided a certain time on bar tops and at overbanks were also affected
626
by this vigorous chemical weathering. Moreover, mechanical weathering, causing destruction
627
along cleavage planes and leading to grains disintegration, certainly affected the mechanically
628
unstable feldspars during this prolonged fluvial transport. Under such conditions of active
629
chemical and physical weathering, all the unstable feldspars and rhyolitic rock fragments were
630
totally dissolved or destructed, whereas the more stable quartz survived, thus giving rise
631
ultimately to the super mature first-cycle quartzarenite. Such a super mature first-cycle
632
quartzarenite is recorded in various cases formed under similar conditions (Van Andel, 1959;
633
Pettijohn, 1975; Mack, 1984, Dickinson, 1985; Garzanti et al., 2013).
634
32
635
7.4. Sandstone suite number 4: Hiswa, Dubaydib, Mudawwara, and Khusha Formations of Early
636
Ordovician to early Silurian age
637
Sandstone suite number 4 consisting of Lower Ordovician Hiswa, Middle-Upper Ordovician
638
Dubaydib, Upper Ordovician-lower Silurian Mudawwara, and lower Silurian Khusha Formations
639
has invariably a subarkosic arenite composition (Fig. 6, Table 2). The depositional environment
640
is marine, fluctuating between the intertidal-subtiadal, and the deep offshore zones.
641
It can be seen from the QtFL and QmFLt compositional diagrams (Figs. 11A, B) that the
642
means of these parameters for the Hiswa Formation fall in the craton interior continental block
643
provenance field, whereas they fall in the transitional continental block provenance field for the
644
Dubaydib, the Mudawwara and the Khusha Formations. The inferred transitional continental
645
block provenance terrane seems to be erroneous. This is because it implies a moderate relief of
646
the Arabian Shield source rocks that in turn indicates a moderate tectonic uplift, which is not
647
correct since the study area underwent a tectonic quiescence between the mid Cambrian and the
648
early Carboniferous. Consequently, the relief of the Arabian Shield should be low, thus a stable
649
craton interior provenance terrane of the continental block might be indicated, which is already
650
the provenance type inferred for the underlying Hiswa Formation of the same sandstone suite.
651
Moreover, it could represent a continuation of the provenance terrane for the preceding
652
sandstone suite, which was similarly deposited under the same tectonic quiescence. How can the
653
framework modes of the present sandstone suite (Table 2) be interpreted in terms of this
654
indicated craton interior provenance terrane?
33
655
The granitiods and gneissic source rocks of this stable craton interior with the
656
characteristic low relief contributed the necessary feldspars that managed somehow to reach the
657
marine depositional environment. Although the rate of erosion was low, the released unstable
658
feldspar grains were not attacked or dissolved neither at the source rocks nor through transit.
659
This is attributed to the absence of chemical weathering during deposition of the present
660
sandstone suite, which, on the contrary, persisted during the time of all the preceding sandstone
661
suites. The reason beyond that is the cold arid or semiarid climate prevailing under the well-
662
known Late Ordovician glacial event that affected the study area within northeast Gondwana
663
(Abed et al., 1993), hens the acting weathering was mechanical rather than chemical. Moreover,
664
the feldspar grains were transported a very short distance by braided rivers to the adjacent
665
shallow marine depositional basin (see position of profiles (outcrops) number 5-11 that are very
666
close to the Arabian Shield, Fig. 2), thus they were not destroyed mechanically. Additionally, the
667
marine environment was gentle or mild on these labile feldspars. Under these conditions of
668
complete absence of chemical weathering and insignificant mechanical weathering, the unstable
669
feldspars, besides the stable quartz gave rise ultimately to the immature subarkosic arenites of
670
the sandstone suite.
671
It can be concluded here, that the erroneous inference of the transitional provenance
672
terrane of the continental block for the Dubaydib, the Mudawwara, and the Khusha Formations
673
applying Dickinson‘s plate tectonic-provenance approach is attributed to the rather unusual
674
influence of the glacial paleo climate.
675
34
676
7.5. Sandstone suite number 5: Kurnub Group of Early Cretaceous age
677
Sandstone suite number 5 consists of the Lower Cretaceous Kurnub Group, and is remarkably
678
composed of a mature quartzarenite (Table 2, Fig. 6). Both of the QtFL and QmFLt
679
compositional diagrams display unequivocal craton interior provenance terrane of the continental
680
block (Figs. 11A, B). This inferred provenance terrane fits very well with the petrographic data
681
and observations recorded here. The detrital framework modes consist almost totally of the two
682
quartz varieties (Qt= 99.7%, Table 2), with a very low feldspar mode (F= 0.3%, Table 2), and
683
can be satisfactorily attributed to the inferred craton interior provenance terrane in hand with the
684
other secondary factors.
685
Similar to the previous four sandstone suites, the provenance terrane is the Arabian
686
Shield in the craton interior within the NE Gondwana continental block. However, lower
687
Paleozoic and lower-middle Mesozoic platform strata flanking this shield contributed the great
688
proportion of recycled sandy detritus according to the following argument. The proposed
689
Arabian Shield provenance terranes at the beginning of the Early Cretaceous was subjected to
690
uplift of the block faulted continental block due to continued breakup and rifting in NE
691
Gondwana, and an associated deep erosion. This tectonic uplift ceased gradually through the
692
Early Cretaceous Epoch, so that the relief of the Arabian Shield, as well as the Paleozoic and
693
older Mesozoic platform clastic strata became low, thus corresponding to the craton interior
694
provenance terrane of the continental block. Consequently, the retarded rate of erosion
695
contributed a wide spectrum of recycled sandy detritus including the monocrystalline and
696
polycrystalline quartz, K-feldspars, and plagioclase. They were subjected to an intense chemical
35
697
weathering due to the hot humid climate prevailing at the source rocks, during the long transit by
698
braided to low sinuosity streams that dispersed from the south-located Arabian Shield to the
699
north-located Neo-Tethys across continental surfaces of low slope. The humid hot or temperate
700
climate in the Early Cretaceous is indicated from the presence of carbonaceous shales and
701
lignites that are interbedded at several stratigraphic positions through the Kurnub Group (Amireh
702
and Abed, 1999). Moreover, the position of Jordan was located within the tropical zone during
703
the Early Cretaceous (Boucot et al., 2013).
704
This vigorous chemical weathering also acted at the depositional sites of the low-lying
705
braidplains, point bars, overbanks, and floodplains (Amireh, 1997, 2000; Amireh and Abed,
706
1999). Moreover, the recycled detritus was as well subjected to mechanical disintegration of the
707
labile feldspar grains along cleavage planes during the prolonged transport pathways. Under
708
these conditions of vigorous chemical weathering, and pronounced mechanical weathering,
709
acting on the recycled detritus, almost all the unstable feldspar grains and rock fragments were
710
destroyed, rendering the residual sediments only to the stable quartz varieties that gave rise
711
ultimately to the mature quartzarenites. However, some of the feldspar grains derived directly
712
from the granitoids and gneisses of the Arabian Shield (not recycled) might have escaped this
713
chemical and mechanical weathering and reached the marine intertidal-subtidal depositional
714
environment in Northern Jordan (profiles number 17-20, Fig. 2) to be deposited within the Jarash
715
and the Bir Fa‘as Formations (Appendix A.12).
716 717
Derivation of the detritus recycled from the Paleozoic and the older Mesozoic formations, or in other words, second-, or probably multi-cyclic origin of the major part of the sandstone
36
718
suite is indicated by the presence of two envelopes of syntaxial quartz overgrowths surrounding
719
the detrital quartz core (Fig. 7F). They represent two successive diagenetic stages that certainly
720
indicate two cycles of sedimentation. Moreover, the well roundness and the well sorting of the
721
quartz grains (Amireh, 2015) may substantiate the recycling origin of the sandstone. This is also
722
supported by detrital zircon U-Pb geochronology of the Lower Cretaceous sandstone of the
723
Kurnub Group west of study area (Kolodner et al., 2009). However, direct derivation of the
724
detritus from the Arabian Shield, and thus a first-cycle origin, cannot be excluded according to
725
the presence of few non-abraded, euhedral detrital zircon grains within the heavy mineral
726
fraction (Fig. 10E), and probably to the occurrence of some feldspar grains. The latter figure
727
shows that the majority of the heavy mineral grains consist of well-rounded, abraded zircon
728
grains that were probably recycled from the older sandstones.
729
730
8. Conclusions
731
1) The lower part of the uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan
732
constitutes a segment of the vast lower Paleozoic siliciclastic platform blanketing northern
733
Gondwana.
734
2) The Arabian Shield craton interior or the transitional group within the NE Gondwana
735
continental block represent the provenance terranes controlled by plate tectonics.
37
736
3) Braided rivers transported huge amounts of siliciclastic sediments and flew towards the north-
737
situated Paleo then Neo-Tethys during the early Paleozoic and the Early Cretaceous,
738
respectively.
739
4) Detrital framework modes of the siliciclastic sequence can be interpreted primarily in terms of
740
Dickinson‘s provenance terranes governed by plate tectonics.
741
5) The inferred recycled orogenic and magmatic arc provenances seem to be erroneous, due to
742
derivation of detritus from local syn-rift rhyolitic extrusions, not represented by plate tectonics-
743
provenance diagrams.
744
6) Immature rhyolitic litharenites and subarkosic arenites are interpreted in terms of basement
745
uplift continental block/local rhyolite extrusion, and transitional group provenances, respectively.
746
7) Super mature first-cycle, and second-cycle quartzarenites, were derived from stable carton
747
interior, and platform strata provenances, respectively, subjected to intense chemical weathering.
748
8) This work recommends to use Dickinson‘s petrographic model elsewhere with caution in
749
cases of intracratonic syn-rift volcanic provenances not represented in the plate tectonics-
750
provenance diagrams, and in cases of extraordinary effect of glacial paleoclimate.
751
752
753
38
754
Acknowledgments
755
The Deanship of Academic Research of the University of Jordan funds the research. Miss. Saja
756
Abu Taha is acknowledged for her assistance in the field and laboratory works, drawing the
757
graphs, and preparing the figures. Thanks for two anonymous reviewers for their valuable
758
comments that improved the paper, and for the editorial team of the Journal of Asian Earth
759
Sciences for their patience during the various phases of manuscript‘s review.
760
761
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Kröner, A., 1984. Late Precambrian Plate Tectonic and Orogeny: A Need to Redefine the Term Pan-African. In: Klerks, J., Michot, J. (Eds.), African Geology, Tervuren, pp. 24-28.
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Kröner, A., Eyal, M., Eyal, Y. 1990. Early Pan-African evolution of the basement around Elat,
1017
Israel, and the Sinai Peninsula revealed by single zircon evaporation dating, and implications
1018
for crustal accretion rates. Geology, 18, 545–8.
1019
1020 1021
Mack, G.H., 1984. Explanations to the relationship between plate tectonics and sandstone composition. J. Sed. Petrol., 54, 212-220.
1022
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Makhlouf, I.M., 1988. Storm-generated channels in the Middle Dubaydib Sandstone Formation, South Jordan. J. of King Saud University, 10, 61-77.
1025
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Marsaglia, K.M., Ingersoll, R.V., 1992. Compositional trends in arc-related, deep-marine sand
1027
and sandstone: a reassessment of magmatic-arc provenance. Geol. Soc. Am. Bull., 104,
1028
1637-1649.
1029
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McGillivray, G.J., Husseini, M.I., 1992. The Paleozoic Petroleum Geology of Central Saudi Arabia. AAPG Bull, 76, 1473-1490.
1032
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Morag, N., Avigad, D., Gerdes, E., Harlavan, Y., 2012. 1000–580 Ma crustal evolution in the
1034
Northern-Arabian Shield revealed by U–Pb–Hf of detrital zircons from late Neoproterozoic
1035
sediments (Elat area, Israel). Precambrian Res., 208–211,197–212.
1036
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Nasiri Bezenjani, R., Pease, V., Whitehouse, M.J., Shalaby, M.H., Kaki, K.A., Kozdroj, W.,
1038
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1039
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1040
regional collision tectonics. Precambrian Res., 245, 225-243.
1041
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Petters, S., 1991. Regional Geology of Africa. Springer-Verlag, 722 pp.
1043
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Pettijohn, F.J., 1975. Sedimentary Rocks, 3rd ed. Harper and Row, New York.
1045 1046
Pettijohn, F.J., Potter, P.E., Siever, R., 1987. Sand and sandstone, 2nd. ed. Springer, New York.
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1048 1049
Powell, J.H., 1989. Stratigraphy and Sedimentation of the Phanerozoic Rocks in Central and South Jordan, Part A Ram and Khreim Groups. NRA Bull.11, Amman, 72 pp.
1050
1051 1052
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1053
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1059 1060
1061
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1063
of conglomerate clasts from the volcano-sedimentary sequence at Wadi Rutig in southern
1064
Sinai, Egypt, as revealed by SIMS U–Pb dating of zircon. Gondwana Res., 20, 450–464.
1065
1066
Schmidt, D.L., Hadley, D.G., Stoeser, D.B., 1979. Late Proterozoic crustal history pf the Arabian
1067
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1068
Abdulazizi University, Jeddah, pp. 41-58.
1069
1070
Schneider, W., Abed, A.M., Salameh, E., 1984. Mineral content and diagenetic pattern tools for
1071
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1072
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1073
1074 1075
Schneider, W., Amireh, B.S., Abed, A.M., 2007. Sequence analysis of the Early Paleozoic sedimentary systems of Jordan. Z. dt. Ges. Geowiss., 158, 225-247.
1076
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1078
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1079
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1082
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1083
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1084
1085 1086
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1087
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1090
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1092
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1093
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1094
1095
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1096
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1097
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58
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1099
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1100
‘Dickinson model’. In: Buccianti, A., Mateu-Figueras, G., Pawlowsky-Glahn, V. (Eds.),
1101
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1102
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1103
1104
Wilde, S., Youssef, K., 2002. A re-evaluation of the origin and setting of the LatePrecambrian
1105
Hammamat Group based on SHRIMP U–Pb dating of detrital zircons from Gebel Umm
1106
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1107
1108
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1109
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1110
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1111
1112
Yaseen, N., Pease, V., Jarrar, Gh., Whitehouse, M., 2013. U-Pb detrital zircon provenance of the
1113
Saramuj Conglomerate, Jordan, and implications for the Neoproterozoic evolution of the Red
1114
Sea. Precambrian Res., 239, 6-23.
1115
59
1116
Zuffa, G.G., 1985. Optical analyses of arenites: influence of methodology on compositional
1117
results. In: Zuffa, G.G. (Ed.), Provenance of Arenites, D. Reidel Publishing Co., the
1118
Netherlands, pp. 165-189.
1119
1120
Figure captions
1121
Fig. 1. A simplified geological map of North Africa and Arabia illustrating the distribution of
1122
Precambrian (cratonic basement, remobilized during Pan African orogeny, Pan African juvenile
1123
crust) outcrops including the Arabian Shield, Nubian Shield, Leo Shield, Saharan Metacraton,
1124
West African Craton, Tanzania-Congo Craton, Paleozoic, Mesozoic sedimentary rocks and
1125
Cenozoic sediments and basalt and sedimentary rocks, and location of study area in Jordan
1126
(modified from Alsharhan and Nairn, 1997 (Paleozoic, Mesozoic and Cenozoic outcrops in
1127
Arabia), Avigad et al., 2003 (Precambrian outcrops in Africa), Johnson et al., 2011 (Precambrian
1128
outcrops in Arabia and Nubia), and Viljoen, 2016 (Paleozoic, Mesozoic and Cenozoic outcrops
1129
in Africa). S= Sarmuj; E= Elat; NG= Negev; J= Jibalah; TH= Talbah Group; WH= Wadi Halfa;
1130
T.= terrane.
1131
Fig. 2. Geological map of Jordan demonstrating the outcrops of the Neoproterozoic basement
1132
complex (Aqaba and Araba Complexes), and Neoproterozoic Aheimir Volcanic Suite; outcrops
1133
of the Cambrian, Ordovician, and Silurian Systems, Lower Cretaceous Series (modified from
1134
Amireh, 2000, Amireh et al., 2001); paleocurrent directions during late Ediacaran-early
1135
Cambrian (pink colored arrow), Cambrian (purple colored arrows), Ordovician (red colored
60
1136
arrows), Early Cretaceous (black colored arrows); position of HM-2, AJ-1, NH-1, and WS-3 oil
1137
discovering wells, and position of investigated profiles: 1= Salab Fm.; 2= Umm Ishrin Fm.; 3=
1138
Disi Fm.; 4= Umm Saham Fm.; 5= Hiswa Fm.; 6= Dubaydib Fm.; 7= Tubailiyat Mb. of
1139
Mudawwara Fm. and KG; 8= Ammar Mb.; 9= Batra Mb. and KG, 10= Ratya Mb.; 11= Khusha
1140
Fm.; 12= Abu Khusheiba Fm. and Umm Ghaddah Fm.; 13= Umm Ghaddah Fm. in Wadi Umm
1141
Ghaddah; 14= Salab Fm., Burj Fm., Abu Khusheiba Fm., Umm Ishrin Fm., and KG in Dana
1142
area; 15= KG in Wadi Karak; 16= Umm Ghaddah Fm. in Wadi Al Mahrakah: 17= KG in Na‘ur;
1143
18= KG in Jarash; 19= KG in A‘arda; 20= KG in O‘ion Musa; S= Sarmuj Conglomerate Fm;
1144
Fm.= Formation; Mb.= Member; KG= Kurnub Group.
1145
Fig. 3. Stratigraphic subdivisions of the uppermost Ediacaran-Lower Cretaceous clastic sequence
1146
of Jordan, and the five sandstone suites (sandstone suite #1- sandstone suite #5) assigned in the
1147
present study.
1148
Fig. 4. Outcrop photographs for some of the formations of the uppermost Ediacaran-Lower
1149
Cretaceous clastic sequence.
1150
(A) Irregular contact (paleorelief) between the upper Ediacaran Aheimir Volcanic suite and the
1151
uppermost Ediacaran-lower Cambrian Umm Ghaddah Formation; person as scale is ca 1.8 m.
1152
(B) Nonconformity (Rum unconformity, Powell et al., 2014) in form of a peneplain (arrow)
1153
between the Neoproterozoic Aqaba Complex and the Fortunian Salab Formation; width of
1154
outcrop is ca 500 m.
61
1155
(C) Contacts between the Neoproterozoic Aqaba Complex, Salab, Burj, Abu Khusheiba, and
1156
Umm Ishrin Formations in Dana Area (profile number 14); height of the tree at lower central part
1157
of the photo attains ca 1.5 m.
1158
(D) Deformed cross-bedding characterizing Umm Ishrin Formation, pencil is ca 15 cm.
1159
(E) A storm channel interbedded within intertidal flat facies of Dubaydib Formation, width of
1160
outcrop is ca 15 m.
1161
(F) A volcanic tuff and a volcaniclastic conglomerate interbedded within the cross-bedded
1162
(CBSS) and horizontal bedded (HBSS) sandstone of the Burj Formation; length of geologic
1163
hammer is 30 cm.
1164
Fig. 5. Tectono sedimentary block diagrams illustrating development of the tectonic-controlled
1165
provenance and the depositional environments through time slices of the late Ediacaran-Late
1166
Cretaceous, corresponding to the five sandstone suites; C.B.= continental block.
1167
(A) Late Ediacaran-early Cambrian time of Umm Ghaddah Formation (SS suite #1). Violet
1168
arrows indicate direction of regional crustal extension (modified from Amireh et al., 2008).
1169
(B) Early-mid Cambrian time of Salab, Abu Khusheiba and Burj Formations (SS suite #2)
1170
(modified from Amireh et al., 1994b).
1171
(C) Late Cambrian-Mid Ordovician time of Umm Ishrin, Disi and Umm Saham Formations (SS
1172
suite #3). CH= channel architectural element, LS= laminated sand sheet, DA= downstream
1173
accretion macroform, FF= over bank fine sediments (modified from Amireh et al., 2001).
62
1174
(D) Mid Ordovician-mid Silurian time of Hiswa, Dubaydib, Mudawwara, and Khusha
1175
Formations (SS suite #4). SF= sandy tidal flat, MF= mixed tidal flat (modified from Amireh et
1176
al., 2001).
1177
(E) Early Cretaceous time of Jarash Formation of the Kurnub Group (SS suite #5) (modified
1178
from Amireh and Abed, 1999).
1179
Fig. 6. Modified sandstone classification of Pettijohn et al. (1987) depicting the types of
1180
sandstone for the means of the members, formations, and groups of the clastic sequence under
1181
investigation; Q= total quartz, F= total feldspars, R= lithic fragments (L).
1182
Fig. 7. Thin section photomicrographs illustrating:
1183
(A) Quartzarenite of Umm Ishrin Formation showing detrital matrix (M) filling passively
1184
interstitial spaces between detrital monocrystalline quartz grains (Qm) without altering the quartz
1185
detrital cores (Qdc)or even the quartz overgrowths (Qog), plane polarized light.
1186
(B) Quartzarenite of Ramel Formation of the Kurnub Group illustrating quartz overgrowth
1187
cement (Qov) filling completely interstitial spaces between detrital monocrystalline quartz grains
1188
without altering them, crossed polarized light.
1189
(C) Quartzarenite of Umm Saham Formation showing iron oxide cement (FeC) filling passively
1190
interstitial spaces between detrital quartz grains (Qm) without altering the quartz grains, pore
1191
space (PS) is left without being filled with cement, plane polarized light.
63
1192
(D) Subarkosic arenite of Dubaydib Formation showing dolomite cement (DC) that corrodes the
1193
framework grains of quartz (Qcorr) and feldspar grains (F) but keeping them unaltered to be
1194
correctly identified, air bubble (AB), crossed polarized light.
1195
(E) Quartzarenite of Karak Formation of the Kurnub Group consisting entirely of quartz
1196
framework grains, particularly monocrystalline quartz cemented by calcite (CC); note corrosion
1197
of a quartz grain (Qcorr) leaving just two patches that are still identifiable (at complete extinction
1198
position), crossed polarized light.
1199
(F) Second-cycle quartzarenite of Karak Formation of the Kurnub Group consisting of
1200
monocrystalline quartz grains characterized by two stages of syntaxial quartz overgrowths. The
1201
first stage overgrowth is separated from the detrital core (Qdc) by the dust line number 1 (DL
1202
#1), and the second stage overgrowth is separated from the first stage by the dust line number 2
1203
(DL #2), crossed polarized light.
1204
Fig. 8. Thin section photomicrographs illustrating:
1205
(A) A polycrystalline quartz (Qp) consisting of equigranular quartz crystals of probably a
1206
metamorphic sandstone origin, and a monocrystalline quartz (Qm) in quartzarenite of Umm
1207
Ishrin Formation, crossed polarized light.
1208
(B) A polycrystalline quartz grain (Qp) consisting of quartz crystals with sutured contacts and a
1209
preferred orientation indicating a foliated metamorphic origin in rhyolitic litharenite of Umm
1210
Ghaddah Formation, crossed polarized light.
64
1211
(C) Chert lithic fragment (Ch) characterized by the clear appearance of quartz and the
1212
microcrystalline texture, and a devitrified rhyolitic lithic fragment (DRL) distinguished by the
1213
brownish turbid appearance and the felsitic texture consisting of cryptocrystalline quartz crystals
1214
smaller than that of chert, in rhyolitic litharenite of Umm Ghaddah Formation, plane polarized
1215
light.
1216
(D) Same as Fig. 8C but under crossed polarized light. Note the obvious contrast between the
1217
quartz microcrystals in extinction and illumination positions characterizing the chert lithic
1218
fragment.
1219
(E) Orthoclase grains (Or) with multiple twinning (mt) and simple twinning (st), and
1220
monocrystalline quartz (Qm) in subarkosic arenite of the Salab Formation, crossed polarized
1221
light.
1222
(F) A microcline grain (Mc) characterized by cross-hatching twinning and monocrystalline
1223
quartz (Qm) and another feldspar grain (F) in a subarkosic arenite of the Salab Formation with,
1224
crossed polarized light.
1225
Fig. 9. Thin section photomicrographs showing:
1226
(A) A devitrified rhyolitic lithic fragment (DRL) with glass shards (GS) that are also devitrified,
1227
and a chert fragment (Ch) in rhyolitic litharenite of Umm Ghaddah Formation, plane polarized
1228
light.
65
1229
(B) Same as Fig. 9A but under crossed polarized light. Note the devitrification of both the
1230
rhyolitic clast (DRL) and the included glass shards (GS) giving rise to microgranular felsitic
1231
texture consisting of cryptocrystalline quartz crystals that are smaller than that of the chert
1232
fragment.
1233
(C) A devitrified rhyolitic lithic fragment (DRL) consisting of phenocrysts (probably an euhedral
1234
feldspar phenocryst, FPhC) and irregular shaped pyroclastic phenocryst (PPhC) that are bound
1235
by a devitrified ground mass (DGM), which is set in a detrital matrix (DtM) in rhyolitic
1236
litharenite of Umm Ghaddah Formation, plane polarized light.
1237
(D) Same as Fig. 9C but under crossed polarized light. Note the devitrification of the phenocrysts
1238
and ground mass within the rhyolitic lithic fragment, and the silt-sized detrital quartz grains in
1239
the detrital matrix.
1240
(E) A rhyolitic lithic fragment exhibiting a spherulitic texture (SphRL) and a devitrified volcanic
1241
lithic fragment (DVL) characterized by microfelsitic texture in rhyolitic litharenite of Umm
1242
Ghaddah Formation, crossed polarized light.
1243
(F) A mafic clast composed of devitrified feldspar laths (DFL) and anhedral phenocryst (APhC)
1244
set in opaque groundmass in rhyolitic litharenite of Umm Ghaddah Formation, plane polarized
1245
light.
1246
Fig. 10. Thin section photomicrographs illustrating:
66
1247
(A) A silty mudstone lithic fragment constituted mainly of silt-sized grains (SSG) and a few fine
1248
sand grains (FSG) bound by a clayey matrix (ClM) in the rhyolitic litharenite of Umm Ghaddah
1249
Formation, plane polarized light.
1250
(B) Same as Fig. 10A but under crossed polarized light. Note the first order interference color of
1251
the silt and sand sized grains, and the cryptocrystalline nature of the clayey matrix.
1252
(C) A schist grain consisting of foliated aggregates of quartz and mica crystals in the rhyolitic
1253
litharenite of Umm Ghaddah Formation, plane polarized light.
1254
(D) Same as Fig. 10C but under crossed polarized light.
1255
(E) Euhedral detrital zircon grain (EZ) derived directly from the Arabian Shield and several
1256
rounded zircon grains (RZ) recycled from Paleozoic and Mesozoic strata, and a rutile grain (R)
1257
in the Karak Formation of the Kurnub Group, grain mount, plane polarized light.
1258
(F) An apatite grain characterized by two stages of apatite overgrowths; apatite overgrowth
1259
number 1 (Aog #1) and apatite overgrowth number 2 (Aog #2) enveloping an apatite detrital core
1260
(Adc) in the subarkosic arenite of Salab Formation, plane polarized light.
1261
Fig. 11. Triangular compositional plots showing mean framework modes for all the members,
1262
formations, and groups of the upper Ediacaran-Lower Cretaceous clastic sequence. (A) QtFL,
1263
(B) QmFLt, (C) QpLvLs, and (D) QmPK. Division lines are after Dickinson and Suczek (1979)
1264
and Dickinson et al., (1983), and in percentage units measured from nearest apical pole. For
1265
number of samples in each member, formation or group see Table 2.
67
1266
1267
Table captions
1268
Table 1. Paleocurrent directions based on 1339 measurements of azimuths of planar and trough
1269
cross bedding (complied from Amireh 1993, 1997, 2000; Amireh et al., 1994a, 2001, 2008;
1270
Amireh and Abed, 1998)
1271
Table 2. Mean, standard deviation (STDEV. S), confidence level (95%) of framework modes for the
1272
members/formations/groups of the uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of
1273
Jordan
1274
1275
Vitae
1276
Belal S. Amireh graduated from the University of Jordan in geology and mineralogy in 1977,
1277
and obtained M.Sc. from the same university in sedimentology and petrography of oil shale in
1278
1979. Amireh received his Ph.D. from the Technical University of Braunschweig in Germany in
1279
sedimentology and petrology of clastic deposits in 1987. He was appointed as an Assistant Prof.
1280
in the University of Jordan in 1991, promoted to an Associate Prof. in 1996, and to a Professor in
1281
2001, where he is still now at this position. Amireh published many articles in international
1282
journals in the field of sedimentology, mineralogy, and geochemistry of clastic deposits.
1283
68
1284 1285
69
1286 1287
70
1288 1289
71
1290 1291
72
1292 1293
73
1294 1295
74
1296 1297
75
1298 1299
76
1300 1301
77
1302 1303
78
1304
79
Table 1. Paleocurrent directions based on 1339 measurements of azimuths of planar and trough cross bedding (complied from Amireh 1993, 1997, 2000; Amireh et al., 1994b, 2001, 2008; Amireh and Abed, 1999)
Age
Form-
Locality
ation
Readings Mean
number
Direction
Age
Form- Locality
Readings Mean
ation
number
direction
LEd-eCamb
UG
W. el Mahrakah
48
55 NE
ECretaceous KG
Mollightah
24
N
Cambrian
S + UI
Rum-Ras Naqab
153
N
ECretaceous KG
W. Dana
33
13 NW
Cambrian
AKh
W. A Khusheiba
96
5 NE
ECretaceous KG
W. Khuneizirah 35
10 NW
Cambrian
S+AKh Dana
113
12 NW
ECretaceous KG
Afra
42
5 NW
Cambrian
S+AKh Safi
12
10 NW
ECretaceous KG
W. el Hasa
28
N
Cambrian
UI
W. Zarq-Ma‘in
44
30 NW
ECretaceous KG
W. Nummeirah
39
5 NW
Ordovician
Disi
Disi-W. Hasa
50
5 NW
ECretaceous KG
W. Isal
38
N
Ordovician
US
G.Gh.-Ras Naqab
77
N
ECretaceous KG
W. el Karak
30
9 NW
Ordovician
Disi
Disi-W.Nummeira 42
6 NW
ECretaceous KG
Hamm. Ma‘in
31
10 NW
W.Mash-W.Karak
12 NW
ECretaceous KG
O‘ion Musa
19
7 NW
ECretaceous KG
80
80
ECretaceous KG
W. Mashabah
6
8 NW
ECretaceous KG
Nau‘r
41
N
ECretaceous KG
Rasen Naqab
14
N
ECretaceous KG
Mahis
20
13 NW
ECretaceous KG
W. Rakeya
3
N
ECretaceous KG
Baqa‘a
42
N
ECretaceous KG
W. Qsieb
23
6 NW
ECretaceous KG
Jarash
53
20 NW
ECretaceous KG
Dillaghah
6
10 NW
ECretaceous KG
A‘arda
77
22 NW
ECretaceous KG
Petra
20
8 NW
Total number of measurements= 1339; LEd-eCamb= late Ediacaran-early Cambrian; ECretaceous= Early Cretaceous; UG= Umm Ghaddah Fm., S= Salab Fm., UI= Umm Ishrin Fm., AKh= Abu Khusheiba Fm., US= Umm Saham Fm., KG= Kurnub Group; for localities of formations or KG see Fig. 2 and Amireh (1993, 2000).
81
Table 2. Mean, standard deviation (STDEV. S), confidence level (95%) of framework modes for the members/formations/groups of the uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan Mb./Fm./G. UG Fm. M (n= 60) STDEV.S C. l. 95% Salab Fm. M (n= 68) STDEV.S C. l. 95% Burj Fm. M (n= 11) STDEV.S C. l. 95% AK Fm. M (n= 20) STD.P C.L.95% UI Fm. M (n= 35) STDEV.S C. l. 95% Disi Fm. M (n= 16) STDEV.S
FW
Mt C
Qt
F
L
Qm
F
Lt
Qp
Lv
Ls
Qm
P
K
81.0 8.8 10.2 43.0 12.6 44.4 38.5 12.6 48.9 10.1 4.9 3.8 4.5 13.0 8.4 16.2 12.1 8.4 15.5 6.6 1.3 1.0 1.2 3.4 2.2 4.2 3.1 2.2 4.0 1.7
82.5 7.4 77.3 8.9 5.7 13.7 2.3 1.5 3.5
2.7 20.0 2.6 11.9 0.7 3.1
80.2 7.9 11.9 77.8 17.2 5.0 5.3 4.3 6.1 10.2 7.4 6.3 1.3 1.0 1.5 2.5 1.8 1.5
29.6 0.4 79.8 28.3 1.9 8.8 7 0.5 2.1
1.4 18.8 1.5 8.2 0.4 2.0
61.9 4.1 88.7 31.6 4.4 4.5 21.2 3.0 3.0
0.5 10.8 0.8 4.7 0.5 3.2
12.9 0.6 88.1 17.2 1.6 5.6 8.3 0.8 2.6
0.6 11.3 0.9 5.2 0.4 2.4
74.1 0.8 25.1 70.5 7.5 7.6 1.5 7.8 20.6 3.8 5.1 1.0 5.2 13.8 2.6
69.2 17.2 13.6 70.0 11 7.4 8.4 28.7 2.7 1.8 2.0 7.1
22.0 65.0 7.5 22.4 19.3 3.8 15.0 13.0 2.6
27.5 34.0 20.9 34.4 14.0 23.1
80.3 5.1 14.6 87.2 11.0 1.8 4.5 5.1 4.2 5.8 4.8 3.6 2.1 2.4 1.9 2.7 2.3 1.7
81.6 11.0 7.4 8.9 4.8 6.4 4.2 2.3 3.0
86.5 18.3 8.8
77.2 3.0 19.8 99.7 0.0 3.5 3.0 4.6 0.8 0.0 1.2 1.0 1.6 0.3
0.3 0.8 0.3
87.1 0.0 8.6 0.0 3.0
12.9 98.1 8.6 4.0 3.0 1.4
1.9 4.0 1.4
0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0
77.3 1.7 21.0 99.7 0.0 5.4 2.5 5.2 0.4 0.0
0.3 0.4
86.1 0.0 9.1 0.0
13.9 98.5 9.1 3.1
1.5 3.1
0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0
82
C. l. 95% US Fm. M (n= 25) STDEV.S C. l. 95% Hiswa Fm. M (n= 9) STDEV.S C. l. 95% Dub. Fm. M (n= 31) STDEV.S C. l. 95% Mudw. Fm. M (n= 31) STDEV.S Conf.l.95 Khu. Fm. M (n= 7) STDEV.S C. l. 95% Kurnub G. M (n= 28) STDEV.S C. l. 95%
2.9
1.3 2.8
0.2
83.0 0.6 16.4 99.9 0.0 4.7 1.3 3.7 0.4 0.0 1.9 0.5 1.5 0.2
0.2
4.8
4.8
1.5
1.5
0.1 0.4 0.2
92.3 0.0 4.2 0.0 1.7
7.7 4.2 1.7
99.5 2.4 1.0
0.5 2.4 1.0
0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0
76.0 5.8 18.2 86.2 13.6 0.2 4.4 8.6 8.7 6.0 6.3 0.7 3.4 6.6 6.7 4.6 4.8 0.5
84.4 13.6 2.0 6.4 6.3 2.4 4.9 4.8 1.8
100.0 0.0 0.0 0.0
0.0 85.8 0.0 7.0 5.4
0.6 13.6 1.0 6.3 0.8 4.8
83.7 1.6 14.7 79.4 20.6 0.0 6.7 2.5 7.0 8.4 8.4 0.0 2.5 0.9 2.6 3.1 3.1
76.5 20.6 2.9 8.8 8.4 2.2 3.2 3.1 0.8
100.0 0.0 0.0 0.0
0.0 78.8 0.0 8.8 3.2
0.5 20.7 0.6 8.5 0.2 3.1
81.8 2.3 15.9 78.0 22.0 0.0 7.0 4.1 6.4 5.9 5.9 0.0 2.6 1.5 2.3 2.2 2.2
75.0 22.0 3.0 4.9 5.9 2.5 1.8 2.2 0.9
100.0 0.0 0.0 0.0
0.0 77.3 0.0 5.9 2.2
0.2 22.5 0.4 5.9 0.1 2.2
87.0 0.6 12.4 81.3 18.7 0.0 3.8 1.5 2.7 2.9 2.9 0.0 3.5 1.4 2.5 2.7 2.7
79.9 18.7 1.4 4.6 2.9 1.8 4.3 2.7 1.7
100.0 0.0 0.0 0.0
0.0 80.8 0.0 3.2 3.0
0.3 18.9 0.5 3.0 0.5 2.8
84.4 4.3 11.3 99.7 0.3 7.0 5.6 7.0 0.9 0.9 2.7 2.2 2.7 0.3 0.3
96.2 0.3 2.4 0.9 0.9 0.3
100.0 0.0 0.0 0.0
0.0 99.7 0.0 0.0
0.0 0.3 0.0 0.0
0.0 0.0
3.5 2.4 0.9
Mb.= Member; Fm.= Formation; G.= Group; FW= framework grains; Mt= detrital matrix ; C= total cements; Qt= total quartz; F= total feldspar; L= lithic fragments; Qm= monocrystalline quartz; Qp= polycrystalline quartz; Lt= total lithic grains; Lv= volcanic lithic fragments; Ls= sedimentary lithic fragments; P= plagioclase; K= K-feldspar; M= mean; n= number of samples; UG= Umm Ghaddah; AK= Abu Khusheiba; UI= Umm Ishrin; US= Umm Saham; Dub.= Dubaydib; Mudw.= Mudawwara; and Khu.= Khusha.
83
Appendix A. Mean, standard deviation (STDEV. S), confidence level (95%) of the framework modes for all samples in each of the groups/formations/members of the uppermost EdiacaranLower Cretaceous clastic sequence A.1 Umm Ghaddah Formation S.N. UG3 UG4 UG5 UG6 UG7 UG8 F. B AJ3791 AJ3791 AJ3790 AJ3750 AJ3706 AJ3694 AJ3650 AJ3590 AJ3560 AJ3500 AJ3470 AJ3410 AJ3350 AJ3280 AJ3240 AJ3200 AJ3160 AJ3130 AJ3100 AJ3070 AJ3055 AJ3035 AJ3015 AJ2995 AJ2982 AJ2980 AJ2978 AJ2975 NH3960 NH3850 NH3700 NH3659 NH3656
FW 86 89 87 88 91 87 77 75 75 79 75 84 80 82 79 74 80 79 75 83 87 82 83 79 88 85 84 86 85 84 91 86 87 89 87 80 79 80 86 78
Mt 6 7 5 5 4 4 8 17 5 13 10 0 16 8 7 9 10 10 12 6 4 6 5 4 7 4 7 5 9 6 7 9 10 7 8 12 9 11 8 15
C 8 4 8 7 5 9 15 8 20 8 15 16 4 10 14 17 10 11 13 11 9 12 12 17 5 11 9 9 6 10 2 5 3 4 5 8 12 9 6 7
Qt 13 40 47 2 48 26 60 27 21 18 39 33 44 41 35 45 45 57 49 70 30 62 54 67 53 59 58 54 48 64 65 43 41 44 43 33 27 34 45 46
F 6 1 0 0 1 2 14 0 0 0 9 0 10 9 5 17 14 5 12 6 3 10 12 10 15 7 7 6 12 7 8 6 11 7 14 20 19 18 20 22
L 81 59 53 98 51 72 26 73 79 82 52 67 46 50 60 38 41 38 39 24 67 28 34 23 32 34 35 40 40 29 27 51 48 49 43 47 54 48 35 32
Qm 12 39 45 2 47 26 57 25 17 14 34 25 36 38 29 33 40 53 45 60 28 61 48 58 50 54 49 47 42 57 62 34 37 35 39 30 24 31 37 42
F 6 1 0 0 1 2 14 0 0 0 9 0 10 9 5 17 14 5 12 6 3 10 12 10 15 7 7 6 12 7 8 6 11 7 14 20 19 18 20 22
Lt 82 60 55 98 52 72 29 75 83 86 57 75 54 53 66 50 46 42 43 34 69 29 40 32 35 39 44 47 46 36 30 60 52 58 47 50 57 51 43 36
Qp 1 2 2 0 2 0 9 4 5 5 7 11 14 7 9 23 11 9 9 28 3 4 15 28 9 12 22 15 13 19 7 15 9 15 10 7 5 5 19 11
Lv 93 94 90 97 96 94 86 87 85 88 80 83 77 86 81 68 84 85 88 68 87 83 73 64 81 76 73 72 77 68 74 64 62 71 83 93 93 95 78 86
Ls 6 4 8 3 2 6 5 9 10 7 13 6 9 7 10 9 5 6 3 4 10 13 12 8 10 12 5 13 10 13 19 21 29 14 7 0 2 0 3 3
Qm 67 97 100 100 98 92 80 100 100 100 80 100 78 82 85 66 74 91 78 91 89 86 80 85 77 88 87 89 78 89 89 85 76 84 74 60 56 64 65 66
P 0 0 0 0 0 0 0 0 0 0 3 0 6 5 0 6 5 0 5 0 0 2 2 0 5 0 2 0 4 0 3 0 2 3 4 8 9 3 4 6
K 33 3 0 0 2 8 20 0 0 0 17 0 16 13 15 28 21 9 17 9 11 12 18 15 18 12 11 11 18 11 8 15 22 13 22 32 35 33 31 28
84
NH3653 NH3651 NH3500 NH3391 NH3389 NH3385 HM1450 HM1400 HM1329 HM1275 HM1270 HM1268 HM1197 HM1196 HM1192 WS4527 WS4500 WS4374 WS4300 WS4217 M (n= 60) STDEV.S C. l. 95%
79 76 78 75 78 79 82 81 76 75 80 73 76 81 75 75 77 81 75 75 81.0 4.9 1.3
14 15 14 10 10 13 10 12 17 3 5 7 9 7 7 13 9 11 14 13 8.8 3.8 1.0
7 9 8 15 12 8 8 7 7 22 15 20 15 12 18 12 14 8 11 12 10.2 4.5 1.2
39 45 33 59 42 52 41 42 36 41 33 35 45 35 40 48 48 40 52 43 43.0 13.0 3.4
22 12 26 20 23 25 10 11 21 22 23 20 18 30 24 28 22 25 9 21 12.6 8.4 2.2
39 43 41 21 35 23 49 47 43 37 44 45 37 35 36 24 30 35 39 36 44.4 16.2 4.2
34 42 29 53 37 46 37 33 30 37 31 32 44 35 38 44 44 37 47 39 38.5 12.1 3.1
22 12 26 20 23 25 10 11 21 22 23 20 18 30 24 28 22 25 9 21 12.6 8.4 2.2
44 46 45 27 40 29 53 56 49 41 46 48 38 35 38 28 34 38 44 40 48.9 15.5 4.0
14 6 8 21 13 22 9 16 11 10 3 6 2 0 7 14 11 10 12 10 10.1 6.6 1.7
86 94 89 79 87 78 82 73 81 73 86 82 93 96 93 76 85 90 82 83 82.5 8.9 2.3
0 0 3 0 0 0 9 11 8 17 11 12 5 4 0 10 4 0 6 7 7.4 5.7 1.5
62 78 53 73 62 64 79 75 59 63 58 62 70 55 62 60 67 60 83 66 77.3 13.7 3.5
2 0 7 2 4 5 3 0 5 2 7 5 2 7 2 6 4 6 0 5 2.7 2.6 0.7
36 22 40 25 34 31 18 25 36 35 35 33 28 38 36 34 29 34 17 29 20.0 11.9 3.1
Qt 68 78 85 88 71 80 82 82 78 94 81 86 87 61 67 69 85 70
F 29 19 15 12 26 19 15 18 18 6 7 5 13 29 32 16 12 23
L 3 3 0 0 3 1 3 0 4 0 12 9 0 10 1 15 3 7
Qm 55 59 70 68 60 78 80 79 75 94 81 86 84 53 57 59 72 65
F 29 19 15 12 26 19 15 18 18 6 7 5 13 29 32 16 12 23
Lt 16 22 15 20 14 3 5 3 7 0 12 9 3 18 11 25 16 12
Qp 79 84 100 100 82 50 50 100 50 0 0 0 100 46 87 41 83 44
Lv 21 16 0 0 18 50 50 0 50 0 100 100 0 54 13 59 17 56
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 66 76 83 85 70 80 84 81 80 94 92 94 87 65 64 78 85 73
P 0 0 0 0 0 3 3 0 3 0 0 0 0 3 5 2 0 5
K 34 24 17 15 30 17 13 19 17 6 8 6 13 32 31 20 15 22
A.2 Salab Formation S.N. SD1 SD2 SD3 SD4 SD5 SD6 SD7 SD8 SD9 SD10 SD11 SD12 SD13 LCD1 LCD2 LCD6 LCD11 LCD14
FW 87 86 81 81 78 77 79 76 83 81 85 91 86 74 75 72 75 74
Mt 6 5 9 9 8 7 9 7 6 8 5 0 5 10 10 10 0 7
C 7 9 10 10 14 16 12 17 11 11 10 9 9 16 15 18 25 19
85
LCD16 LCD20 LCD29 LCD32 SR1 SR2 SR3 SR4 SR5 SR6 SR11 LCR3 LCR5 LCR6 LCR7 LCR9 LCR14 LCR18 AJ2930 AJ2880 AJ2820 AJ2780 AJ2760 AJ2710 AJ2680 AJ2640 AJ2600 NH3100 NH3000 NH2867 NH2866 NH2864 NH2860 NH2400 HM953 HM882 HM798 HM680 HM582 HM428 HM420 HM410 WS4200 WS4150 WS4050 WS3950 WS3850 WS3800
79 76 73 78 73 77 78 75 76 80 75 83 76 75 76 78 80 76 87 91 86 88 85 87 90 84 83 78 75 77 81 77 74 77 84 91 92 88 91 82 79 80 81 76 81 77 78 75
0 0 16 3 9 8 10 10 9 6 10 1 2 2 3 3 0 0 10 8 12 11 13 7 4 12 11 12 13 11 8 8 17 15 11 5 4 8 5 8 8 10 10 14 12 15 12 12
21 24 11 19 18 15 12 15 15 14 15 16 22 23 21 19 20 24 3 1 2 1 2 6 6 4 6 10 12 12 11 15 9 8 5 4 4 4 4 10 13 10 9 10 7 8 10 13
67 86 79 85 89 77 64 80 79 94 50 86 81 70 73 81 82 92 72 81 81 84 86 79 89 92 71 46 63 61 64 60 74 81 73 85 87 87 93 82 78 92 73 68 79 72 85 68
6 14 21 15 8 18 29 20 21 6 26 14 19 30 27 19 18 8 13 9 19 13 9 21 7 6 24 32 24 23 20 26 18 19 19 10 8 6 5 17 18 8 20 24 12 22 15 29
27 0 0 0 3 5 7 0 0 0 24 0 0 0 0 0 0 0 15 10 0 3 5 0 4 2 5 22 13 16 16 14 8 0 8 5 5 7 2 1 4 0 7 8 9 6 0 3
48 59 65 81 85 72 54 76 79 94 44 74 76 63 71 72 77 79 70 73 78 78 76 68 75 75 65 44 52 58 55 52 65 71 66 58 77 76 80 72 59 79 64 62 72 61 70 60
6 14 21 15 8 18 29 20 21 6 26 14 19 30 27 19 18 8 13 9 19 13 9 21 7 6 24 32 24 23 20 26 18 19 19 10 8 6 5 17 18 8 20 24 12 22 15 29
46 27 14 4 7 10 17 4 0 0 30 12 5 7 3 9 5 13 17 18 3 9 15 11 18 19 11 24 24 19 25 22 17 10 15 32 15 18 15 11 23 13 16 14 16 17 15 11
42 100 100 100 60 50 59 100 0 0 45 100 100 100 100 100 100 100 13 44 100 62 69 100 75 87 56 11 47 20 37 35 50 100 46 83 64 62 86 89 83 100 54 45 46 62 100 75
58 0 0 0 40 50 41 0 0 0 49 0 0 0 0 0 0 0 87 56 0 38 31 0 25 13 44 89 53 73 63 53 50 0 54 17 36 38 14 11 17 0 46 55 54 38 0 25
0 0 0 0 0 0 0 0 0 0 6 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 7 0 12 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
88 81 75 84 91 80 65 79 79 94 63 83 80 68 73 79 82 90 85 89 81 86 89 76 92 93 73 58 69 71 73 67 78 78 77 85 91 93 95 81 77 91 76 80 75 73 82 67
0 0 5 1 0 0 0 0 1 0 0 3 0 3 1 1 1 2 1 0 2 1 0 3 0 0 3 3 2 3 2 3 3 2 0 2 0 0 0 3 2 0 2 1 3 1 0 3
12 19 20 15 9 20 35 21 20 6 37 14 20 29 26 20 17 8 14 11 17 13 11 21 8 7 24 39 29 26 25 30 19 20 23 13 9 7 5 16 21 9 22 19 22 25 18 30
86
WS3718 WS3713 M (n= 68) STDEV.S C. l. 95%
79 77 80.2 5.3 1.3
3 14 7.9 4.3 1.0
18 9 11.9 6.1 1.5
81 77 77.8 10.2 2.5
19 23 17.2 7.4 1.8
0 0 5.0 6.3 1.5
77 71 69.2 11 2.7
19 23 17.2 7.4 1.8
4 6 13.6 8.4 2.0
C 14 18 28 30 22 18 30 42 27 20 27 25.1 7.8 5.2
Qt 89 84 85 81 90 85 56 76 40 32 58 70.5 20.6 13.8
F 9 16 11 4 5 9 4 5 5 5 9 7.5 3.8 2.6
L 2 0 4 15 5 6 40 19 55 63 33 22.0 22.4 15.0
Qm 75 72 80 74 86 84 54 72 35 29 55 65.0 19.3 13.0
F 9 16 11 4 5 9 4 5 5 5 9 7.5 3.8 2.6
Lt 16 12 9 22 9 7 42 23 60 66 36 27.5 20.9 14.0
F 13 6 15 11 13 10 7 7 5 9 7 10 14 16 6 4
L 0 0 0 0 0 0 0 0 0 0 2 15 7 4 4 3
Qm 84 94 81 88 84 79 93 92 94 90 85 64 73 75 83 85
F 13 6 15 11 13 10 7 7 5 9 7 10 14 16 6 4
Lt 3 0 4 1 3 11 0 1 1 1 8 26 13 9 11 11
100 100 70.0 28.7 7.1
0 0 29.6 28.3 7
0 0 0.4 1.9 0.5
80 75 79.8 8.8 2.1
1 3 1.4 1.5 0.4
19 22 18.8 8.2 2.0
A.3 Burj Formation S.N. MCD29 MCD32 MCD38 MCD34 MCD42 MCD43 MCD44 MCD50 B1 B3 B4 M (n= 11) STDEV.S C. l. 95%
FW 81 81 70 70 77 82 70 56 73 80 73 74.1 7.6 5.1
Mt 5 1 2 0 1 0 0 0 0 0 0 0.8 1.5 1.0
Qp 92 100 50 32 43 17 4 15 9 4 8 34.0 34.4 23.1
Lv 8 0 50 60 57 83 86 77 89 86 85 61.9 31.6 21.2
Ls 0 0 0 8 0 0 10 8 2 10 7 4.1 4.4 3.0
Qm 89 82 87 94 94 91 92 93 86 82 85 88.7 4.5 3.0
P 2 0 2 1 0 0 0 0 0 0 0 0.5 0.8 0.5
K 9 18 11 5 6 9 7 7 14 18 15 10.8 4.7 3.2
A.4 Abu Khusheiba Formation S.N. AK1 AK2 AK3 AK4 AK5 Ak6 AK7 AK8 AK9 AK10 MCKS2 MCKS6 MCKS10 MCKS13 MCKS16 MCKS18
FW 78 83 82 85 75 74 75 75 83 82 86 89 76 83 84 80
Mt 8 5 5 5 7 8 9 9 0 0 2 0 8 0 1 10
C 14 12 13 10 18 18 16 16 17 18 12 11 16 17 15 10
Qt 87 94 85 89 87 90 93 93 95 91 91 75 79 80 90 93
Qp 100 0 100 100 100 100 0 100 100 100 71 43 50 57 67 78
Lv 0 0 0 0 0 0 0 0 0 0 29 48 45 43 33 22
Ls 0 0 0 0 0 0 0 0 0 0 0 9 5 0 0 0
Qm 87 94 85 89 87 89 93 93 95 91 93 86 83 83 93 96
P 0 0 0 0 0 0 0 0 0 0 1 2 2 1 0 0
K 13 6 15 11 13 11 7 7 5 9 6 12 15 16 7 4
87
MCKS21 MCDII1 MCDII5 MCDI10 M (n= 20) STD.P C.L.95%
86 75 75 80 80.3 4.5 2.1
0 21 0 5 5.1 5.1 2.4
14 4 25 15 14.6 4.2 1.9
89 85 79 79 87.2 5.8 2.7
9 15 21 21 11 4.8 2.3
2 0 0 0 1.8 3.6 1.7
79 71 67 71 81.6 8.9 4.2
9 15 21 21 11 4.8 2.3
12 14 12 8 7.4 6.4 3
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
L 0 0 0 0 0 0 0 0 0 0 0 0 0 1 1 0 3 0 0 0 3 1 0 0 0 0 0 1 0 0 1 0
Qm 92 100 95 93 92 100 97 94 96 97 94 97 90 75 70 79 77 82 78 84 78 88 82 83 78 85 78 77 75 100 88 91
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Lt 8 0 5 7 8 0 3 6 4 3 6 3 10 25 30 21 23 18 22 16 22 12 18 17 22 15 22 23 25 0 12 9
80 100 100 100 86.5 18.3 8.8
20 0 0 0 12.9 17.2 8.3
0 0 0 0 0.6 1.6 0.8
90 82 76 77 88.1 5.6 2.6
1 3 1 1 0.6 0.9 0.4
9 15 23 22 11.3 5.2 2.4
Lv 0 0 0 0 0 0 0 0 0 0 0 0 0 6 5 0 12 0 0 0 12 11 0 0 0 0 0 6 0 0 10 0
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100
P 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
K 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
A.5 Umm Ishrin Formation S.N. UI1 UI9A UI10 UI12 UI13 UI14 UI15 UI17 MCD15 MCD20 MCD23 MCD28 CR1 CR3 CR5 CR8 CR10 CR14 CR17 CR24 CR27 CR33 CR37 CR40 CR41 CR46 CR49 CR55B CR60 AK12 MCKS23 LCR22
FW 89 82 80 75 74 73 77 80 77 71 77 75 79 74 76 75 76 76 76 75 79 76 75 75 82 74 78 77 75 80 82 73
Mt 2 4 2 5 5 0 7 6 0 2 5 7 6 5 4 6 12 1 8 0 2 0 0 1 1 0 1 0 0 0 0 0
C 9 14 18 20 21 27 16 14 23 27 18 18 15 21 20 19 12 23 16 25 19 24 25 24 17 26 21 23 25 20 18 27
Qt 100 100 100 100 100 100 100 100 100 100 100 100 100 99 99 100 97 100 100 100 97 99 100 100 100 100 100 99 100 100 99 100
Qp 100 0 100 100 100 0 100 100 100 100 100 100 100 94 95 100 88 100 100 100 88 89 100 100 100 100 100 94 100 0 90 100
88
SR8 SR9 SR10 M (n= 35) STDEV.S C. l. 95%
77 82 79 77.2 3.5 1.2
4 6 3 3.0 3.0 1.0
19 12 18 19.8 4.6 1.6
100 100 100 99.7 0.8 0.3
0 0 0 0.0 0.0
0 0 0 0.3 0.8 0.3
89 95 81 87.1 8.6 3.0
0 0 0 0.0 0.0
11 5 19 12.9 8.6 3.0
100 100 100 98.1 4.0 1.4
0 0 0 1.9 4.0 1.4
0 0 0 0.0 0.0
100 100 100 100.0 0.0
0 0 0 0.0 0.0
0 0 0 0.0 0.0
C 23 21 23 23 11 8 21 25 26 25 24 25 22 15 20 24 21.0 5.2 2.8
Qt 100 100 100 100 100 100 100 100 99 99 100 99 100 100 99 100 99.7 0.4 0.2
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
L 0 0 0 0 0 0 0 0 1 1 0 1 0 0 1 0 0.3 0.4 0.2
Qm 96 96 100 97 100 78 81 72 77 80 87 76 86 86 85 81 86.1 9.1 4.8
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
Lt 4 4 0 3 0 22 19 28 23 20 13 24 14 14 15 19 13.9 9.1 4.8
Qp 100 100 0 100 0 100 100 100 94 100 100 94 100 100 91 100 98.5 3.1 1.5
Lv 0 0 0 0 0 0 0 0 6 0 0 6 0 0 9 0 1.5 3.1 1.5
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
Qm 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100.0 0.0
P 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
K 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
F 0 0 0 0 0 0 0 0 0 0
L 0 0 0 0 0 0 0 0 0 2
Qm 96 91 92 96 93 96 94 94 97 80
F 0 0 0 0 0 0 0 0 0 0
Lt 4 9 8 4 7 4 6 6 3 20
A.6 Disi Formation S.N. DS3 DS4 DS7 DS9 DS15 DS16 O1M4 O1M6 O1M7 O1M9 O1M19 O1M31 O1M32 O1M33 O1M34 O1M39 M (n= 16) STDEV.S C. l. 95%
FW 75 79 74 75 88 92 79 75 74 75 70 75 78 77 75 76 77.3 5.4 2.9
Mt 2 0 3 2 1 0 0 0 0 0 6 0 0 8 5 0 1.7 2.5 1.3
A.7 Umm Saham Formation S.N. US2 US3 US4 US8 US11 US12 US9B H1 H2 LOG4
FW 90 86 97 87 85 73 88 79 83 83
Mt 0 0 0 0 0 0 0 0 0 3
C 10 14 3 13 15 27 12 21 17 14
Qt 100 100 100 100 100 100 100 100 100 98
Qp 100 100 100 100 100 100 100 100 100 88
Lv 0 0 0 0 0 0 0 0 0 12
Ls 0 0 0 0 0 0 0 0 0 0
Qm 100 100 100 100 100 100 100 100 100 100
P 0 0 0 0 0 0 0 0 0 0
K 0 0 0 0 0 0 0 0 0 0
89
LOG8 LOG11 LOG15 LOG21 LOG24 LOG27 LOG30 LOG33 LOG34 LOG37 MOM0 MOM2 MOM5 MOM9 MOM11 M (n= 25) STDEV.S C. l. 95%
83 80 79 80 84 83 83 85 83 84 81 83 77 78 80 83.0 4.7 1.9
5 2 0 1 0 0 0 0 0 0 0 0 3 0 2 0.6 1.3 0.5
12 18 21 19 16 17 17 15 17 16 19 17 20 22 18 16.4 3.7 1.5
100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 99.9 0.4 0.2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.1 0.4 0.2
89 89 87 94 86 89 87 93 94 96 97 94 96 94 94 92.3 4.2 1.7
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
11 11 13 6 14 11 13 7 6 4 3 6 4 6 6 7.7 4.2 1.7
100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 99.5 2.4 1.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.5 2.4 1.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
Qt 82 82 83 89 91 77 84 95 93 86.2 6.0 4.6
F 18 18 17 11 9 23 16 5 5 13.6 6.3 4.8
L 0 0 0 0 0 0 0 0 2 0.2 0.7 0.5
Qm 82 82 83 89 91 72 80 90 91 84.4 6.4 4.9
F 18 18 17 11 9 23 16 5 5 13.6 6.3 4.8
Lt 0 0 0 0 0 5 4 5 4 2.0 2.4 1.8
Qp 0 0 0 0 0 100 100 100 100 100.0 0.0
Lv 0 0 0 0 0 0 0 0 0 0.0 0.0
Ls 0 0 0 0 0 0 0 0 0 0.0 0.0
Qm 79 82 83 89 91 75 84 95 95 85.8 7.0 5.4
P 1 0 0 0 0 3 1 0 0 0.6 1.0 0.8
K 20 18 17 11 9 22 15 5 5 13.6 6.3 4.8
Qt 86 92 93 84 90 89 90
F 14 8 7 16 10 11 10
L 0 0 0 0 0 0 0
Qm 84 88 91 84 84 85 90
F 14 8 7 16 10 11 10
Lt 2 4 2 0 6 4 0
Qp 100 100 100 0 100 100 0
Lv 0 0 0 0 0 0 0
Ls 0 0 0 0 0 0 0
Qm 86 92 93 84 90 88 90
P 0 0 0 0 0 0 0
K 14 8 7 16 10 12 10
A.8 Hiswa Formation S.N. H4 H5 H6 H7 H9 MOM15 MOM15A MOM18 MOM20 M (n= 9) STDEV.S C. l. 95%
Fw 70 73 75 76 78 77 75 86 74 76.0 4.4 3.4
Mt 14 0 25 0 3 8 0 2 0 5.8 8.6 6.6
C 16 27 0 24 19 15 25 12 26 18.2 8.7 6.7
A.9 Dubaydib Formation S.N. D1 D3 D5 D7 D8 D10 D12
FW 86 90 90 80 70 87 87
Mt 2 0 0 0 0 0 0
C 12 10 10 20 30 13 13
90
D13 D15 D17 D19 D22 D23 DMZ2 DMZ7 DMZ13 DMZ14 DMZ16 UOK0 UOK1 UOK6 UOK11 UOK15 UOK17 UOK21 UOK23 UOK25 UOK28 UOK31 UOK34 UOK35 M (n= 31) STDEV.S C. l. 95%
87 90 88 90 86 86 93 82 93 90 79 81 87 81 88 70 72 84 71 73 82 87 81 84 83.7 6.7 2.5
0 0 0 0 0 0 0 2 1 0 5 9 7 2 2 0 0 4 0 0 7 3 3 1 1.6 2.5 0.9
13 10 12 10 14 14 7 16 6 10 16 10 6 17 10 30 28 12 29 27 11 10 16 15 14.7 7.0 2.6
83 93 86 74 62 64 75 70 83 84 77 70 71 79 73 73 79 77 81 81 85 73 75 69 79.4 8.4 3.1
17 7 14 26 38 36 25 30 17 16 23 30 29 21 27 27 21 23 19 19 15 27 25 31 20.6 8.4 3.1
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
83 90 83 70 62 61 70 68 83 82 77 66 66 77 72 73 77 69 79 78 79 68 69 64 76.5 8.8 3.2
17 7 14 26 38 36 25 30 17 16 23 30 29 21 27 27 21 23 19 19 15 27 25 31 20.6 8.4 3.1
0 3 3 4 0 3 5 2 0 2 0 4 5 2 1 0 2 8 2 3 6 5 6 5 2.9 2.2 0.8
0 100 100 100 0 100 100 100 0 100 0 100 100 100 100 0 100 100 100 100 100 100 100 100 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
83 93 86 73 62 63 74 69 83 84 77 68 70 79 73 72 79 75 80 81 84 71 73 68 78.8 8.8 3.2
0 0 0 0 0 0 0 0 0 0 0 2 1 1 1 1 0 1 1 1 1 1 1 2 0.5 0.6 0.2
17 7 14 27 38 37 26 31 17 16 23 30 29 20 26 27 21 24 19 18 15 28 26 30 20.7 8.5 3.1
F 17 27 20 24 16 28 16 9 19 21 21 24 26 14
L 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 76 71 75 70 82 71 81 83 77 75 77 74 71 81
F 17 27 20 24 16 28 16 9 19 21 21 24 26 14
Lt 7 2 5 6 2 1 3 8 4 4 2 2 3 5
Qp 100 100 100 100 100 100 100 100 100 100 100 100 100 100
Lv 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 82 72 79 74 84 72 84 91 80 78 78 75 73 85
P 0 0 0 0 0 1 1 0 0 0 0 0 0 0
K 18 28 21 26 16 27 15 9 20 22 22 25 27 15
A.10 Mudawwara Formation S.N. TB1 TB5 TB7 TB9 TB11 LS2 LS8 LS11 AM1 AM2 AM4 AM9 BT1 BT4
FW 89 91 86 94 87 82 74 82 77 75 89 90 90 74
Mt 0 0 0 0 0 2 0 1 20 0 0 0 0 3
C 11 9 14 6 13 16 26 17 3 25 11 10 10 23
Qt 83 73 80 76 84 72 84 91 81 79 79 76 74 86
91
LS16 LS18 LS20 LS24 RS1 RS3 RS5 RS6 RS8 RS9 RS10 LS30 LS32 LS34 LS36 LS45 LS48 M (n= 31) STDEV.S Conf.l.95
87 86 87 78 70 74 75 70 76 75 75 81 84 87 89 88 74 81.8 7.0 2.6
0 1 0 6 12 4 5 2 2 3 2 3 1 1 0 2 0 2.3 4.1 1.5
13 13 13 16 18 22 20 28 22 22 23 16 15 12 11 10 26 15.9 6.4 2.3
84 72 84 72 72 75 67 77 78 75 72 88 81 72 85 76 71 78.0 5.9 2.2
16 28 16 28 28 25 33 23 22 25 28 12 19 28 15 24 29 22.0 5.9 2.2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
82 72 82 69 70 71 65 77 74 74 72 84 81 72 75 70 71 75.0 4.9 1.8
16 28 16 28 28 25 33 23 22 25 28 12 19 28 15 24 29 22.0 5.9 2.2
2 0 2 3 2 4 2 0 4 1 0 4 0 0 10 6 0 3.0 2.5 0.9
100 0 100 100 100 100 100 0 100 100 0 100 100 100 100 100 0 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
84 72 84 71 71 74 67 77 77 75 72 87 80 70 83 74 71 77.3 5.9 2.2
1 1 0 0 0 0 0 0 0 0 0 0 0 1 1 1 0 0.2 0.4 0.1
15 27 16 29 29 26 33 23 23 25 28 13 20 28 16 25 29 22.5 5.9 2.2
C 9 10 12 16 12 12 16 12.4 2.7 2.5
Qt 83 84 85 81 77 79 80 81.3 2.9 2.7
F 17 16 15 19 23 21 20 18.7 2.9 2.7
L 0 0 0 0 0 0 0 0.0 0.0
Qm 83 84 85 80 72 77 78 79.9 4.6 4.3
F 17 16 15 19 23 21 20 18.7 2.9 2.7
Lt 0 0 0 1 5 2 2 1.4 1.8 1.7
Qp 0 0 0 100 100 100 100 100.0 0.0
Lv 0 0 0 0 0 0 0 0.0 0.0
Ls 0 0 0 0 0 0 0 0.0 0.0
Qm 83 84 85 80 76 79 79 80.8 3.2 3.0
P 0 0 0 1 1 0 0 0.3 0.5 0.5
K 17 16 15 19 23 21 21 18.9 3.0 2.8
C 10 9
Qt 100 100
F 0 0
A.11 Khusha Formation S.N. KH1 KH2 KH4 S1 S6 S12 S15 M (n= 7) STDEV.S C. l. 95%
FW 91 90 88 80 88 88 84 87.0 3.8 3.5
Mt 0 0 0 4 0 0 0 0.6 1.5 1.4
A.12 Kurnub Group S.N. CrM in CrK2
FW 90 91
Mt 0 0
L 0 0
Qm 98 100
F 0 0
Lt 2 0
Qp 100 0
Lv 0 0
Ls 0 0
Qm 100 100
P 0 0
K 0 0
92
CrK7 CrZ2 CrZ4 CrZ9 CrZ11 CrZ18 CrZ22 CrZ23 CrZ27 CrZ28 CrZ36 CrZ39 CrZ48 CrD5 CrD12 CrD16 CrD19 CrD24 TB13 BT10 K1 KN1 KN3 KN6 R4 R9 M (n= 28) STDEV.S C. l. 95%
78 84 82 78 90 82 84 91 76 81 71 96 73 93 75 74 85 95 87 88 80 88 91 81 90 88 84.4 7.0 2.7
15 0 0 12 0 2 0 0 0 5 1 0 0 0 20 12 6 5 8 6 12 1 2 3 0 11 4.3 5.6 2.2
7 16 18 10 10 16 16 9 24 14 28 4 27 7 5 14 9 0 5 6 8 11 7 16 10 1 11.3 7.0 2.7
100 100 100 96 100 100 100 100 100 100 98 100 98 100 100 100 100 100 100 100 100 100 100 100 100 100 99.7 0.9 0.3
0 0 0 4 0 0 0 0 0 0 2 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0.3 0.9 0.3
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
100 93 99 95 94 98 99 97 92 96 96 96 94 97 91 94 95 97 95 100 95 98 98 95 98 94 96.2 2.4 0.9
0 0 0 4 0 0 0 0 0 0 2 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0.3 0.9 0.3
0 7 1 1 6 2 1 3 8 4 2 4 4 3 9 6 5 3 5 0 5 2 2 5 2 6 3.5 2.4 0.9
0 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 0 100 100 100 100 100 100 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
100 100 100 96 100 100 100 100 100 100 98 100 99 100 100 100 100 100 100 100 100 100 100 100 100 100 99.7 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 4 0 0 0 0 0 0 2 0 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0.3 0.0
93
Graphical abstract
94
Highlights
The study investigates part of the vast N Gondwana lower Paleozoic sandstone sheet It evaluates petrographically the factors governing modal composition of sandstone Provenance controlled by plate tectonics appears to be the primary factor About 50% of the siliciclastic sequence represents a success for Dickinson‘s approach Intracratonic syn-rift extrusion or glacial effects are behind its inapplicability
S1367-9120(17)30709-5 https://doi.org/10.1016/j.jseaes.2017.12.037 JAES 3369
To appear in:
Journal of Asian Earth Sciences
Received Date: Revised Date: Accepted Date:
2 July 2017 25 December 2017 27 December 2017
Please cite this article as: Amireh, B.S., Petrogenesis of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan: provenance, tectonic, and climatic implications, Journal of Asian Earth Sciences (2017), doi: https://doi.org/10.1016/j.jseaes.2017.12.037
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Petrogenesis of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous siliciclastic
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sequence of Jordan: provenance, tectonic, and climatic implications
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Belal S. Amireh
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Dept. of Applied and Environmental Geology
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The University of Jordan
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Amman 11942, Jordan
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[email protected]
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ABSTRACT
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Detrital framework modes of the NE Gondwanan uppermost Ediacaran-Lower Cretaceous
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siliciclastic sequence of Jordan are determined employing the routine polarized light microscope.
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The lower part of this sequence constitutes a segment of the vast lower Paleozoic siliciclastic
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sheet flanking the northern Gondwana margin that was deposited over a regional unconformity
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truncating the outskirts of the East African orogen in the aftermath of the Neoproterozoic
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amalgamation of Gondwana. The research aims to evaluate the factors governing the detrital
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light mineral composition of this sandstone. The provenance terranes of the Arabian craton
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controlled by plate tectonics appear to be the primary factor in most of the formations, which
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could be either directly inferred employing Dickinson‘s compositional triangles or implied
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utilizing the petrographic data achieved and the available tectonic and geological data. The
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Arabian-Nubian Shield constitutes invariably the craton interior or the transitional provenance
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terrane within the NE Gondwana continental block that consistently supplied sandy detritus
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through northward-flowing braided rivers to all the lower Paleozoic formations. On the other
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hand, the Lower Cretaceous Series received siliciclastic debris, through braided-meandering
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rivers having same northward dispersal direction, additionally from the lower Paleozoic and
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lower-middle Mesozoic platform strata in the Arabian Craton. The formations making about
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50% of the siliciclastic sequence represent a success for Dickinson‘s plate tectonics-provenance
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approach in attributing the detrital framework components primarily to the plate tectonic setting
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of the provenance terranes. However, even under this success, the varying effects of the other
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secondary sedimentological and paleoclimatological factors are important and could be crucial.
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The inapplicability of this approach to infer the appropriate provenance terranes of the remaining
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formations could be ascribed either to the special influence of local intracratonic syn-rift
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rhyolitic extrusions, where their plate tectonic setting is not represented by the standard plate
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tectonics-provenance diagrams, or to the rather unusual effect of the Late Ordovician glacial
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event.
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Key words: Framework modes, provenance terranes, Gondwana, Arabian-Nubian Shield, lower
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Paleozoic siliciclastic platform, Jordan, sandstone types
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1. Introduction
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The modal framework composition of siliciclastic sediments and sedimentary rocks is governed
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by several factors including: provenance type, tectonic setting in general and plate tectonics in
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particular, climate and the corresponding type of weathering, mixing of sediments from multiple
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sources, mechanical modifications during transportation, effects of depositional environment,
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and influence of diagenesis generally and intrastratal solution particularly.
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Several publications considered the plate tectonic setting of the provenance the primary
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factor governing the modal framework composition of sandstone (Dickinson and Suczek, 1979;
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Dickinson et al., 1983; Dickinson, 1985, 1988). Other studies confirmed this plate tectonic-
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provenance approach. For instant, Marsaglia and Ingersoll (1992) documented that this model
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works excellently for magmatic arcs. In addition, Ingersoll and Eastmond (2007), and Ingersoll
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(2012) tested Dickinson's petrologic model relating sandstone composition to the dissected
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magmatic arc provenance, employing modern sands from Sierra Nevada drainages, and
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concluded the robust nature of the plate tectonic-provenance axiom.
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On the other hand, some studies criticized Dickinson‘s standard provenance approach,
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and highlighted inconsistent relationship, or disagreement between the modal framework
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composition of some sandstones with the plate tectonic setting inferred by the model (Suttner et
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al., 1981; Mack, 1984). This criticism was limited earlier to specific exceptions, such as
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derivation of clastics from an older tectonic setting, sandstone subjected to intensive weathering
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giving rise to super- or mature sandstone, mixing of two or more provenances or derivation from
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another tectonic setting not represented in the plate tectonic-provenance diagrams, and
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sandstones containing large amounts of detrital carbonate grains (Zuffa, 1985). Therefore, these
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sedimentary petrology schools refused to adopt Dickinson’s petrographic model and focused
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more on the compositional modifications during erosion, transport, deposition, and diagenesis.
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Another criticism to Dickinson‘s model is its establishment mainly upon ancient sandstones,
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where ancient plate tectonic settings, particularly those of the late Ediacaran Epoch, are assumed
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rather than known. Additionally, Weltje (2006) showed that the inferred continental block,
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magmatic arc, and recycled orogenic provenance terranes can be discriminated by Dickinson‘s
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model with a success rate of only 64% to 78%.
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Recently, Garzanti (2016) questioned the validity of inferring plate tectonic setting
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straightforwardly from the models of framework modes of sands and sandstones. It is recorded
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that the detrital modes of sandstones cannot decipher the plate-tectonic setting in which they
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were deposited because petrography alone cannot discriminate allochthonous versus
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autochthonous, orogenic versus anorogenic, or young versus old source rocks. Additionally,
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more substantial flaws were proposed, such as the oversimplification of orogenic domains and
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the disregard of rift related settings, anorogenic volcanism, and ophiolitic sources. Thus, it is
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concluded that the geodynamic setting could not be univocally inferred from the detrital modes
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of sandstone.
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The uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan, the lower
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part of which constitutes a segment of the immense lower Paleozoic siliciclastic platform
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bordering most of northern Gondwana margin, represents a unique case study to evaluate the
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weight of each of the various factors governing the detrital framework composition of sandstone.
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This is due to the high thickness of the sequence (ca 2500 m), and the immense geologic time
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represented spanning from the late Ediacaran to the Late Cretaceous. Moreover, various sorts of
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provenance terranes contributed sand to the sequence through this time. Significantly, the
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tectonic setting evolved from the extensional rifting phase of the Pan African orogeny to a stable
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craton formed in the aftermath of the Neoproterozoic amalgamation of Gondwana and a passive
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continental shelf flanking the southern margin of the Paleo-Tethys, then the Meso-Tethys. In
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addition, the climate changed dramatically from hot humid through cold glacial, then back to
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warm humid. Furthermore, the depositional environment evolved from alluvial fans to proximal-
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distal braidplains, through shallow-deep marine, to sand flats or vast braidplains, to intertidal-
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offshore, and back to braided-meandering rivers.
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Mineral composition of parts of the siliciclastic sequence has been studied by several authors including Schneider et al. (1984, 2007), Khoury (1986), Weissbrod and Nachmias (1986), Amireh (1987, 1991, 1994), Amireh and Abed, 2000, and Amireh et al. (1994a, 2008).
Therefore, the present petrographic investigation aims at employing the uppermost
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Ediacaran-Lower Cretaceous siliciclastic sequence cropping out and sub-cropping in Jordan to
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assess the significance of each of the various factors governing the sandstone detrital framework
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modes. Furthermore, it attempts to answer the question whether plate tectonic setting is the
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primary factor influencing the sandstone‘s detrital light mineral composition.
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2. Geologic setting
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About 2500 meter-thick siliciclastic sequence with subordinate carbonates ranging in age from
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the late Ediacaran to the Late Cretaceous crops out and sub crops in certain parts of Jordan (Figs.
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2, 3). Its lower part constitutes a portion of the vast lower Paleozoic siliciclastic platform
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covering the outskirts of the East African orogen in northern Gondwana (Fig. 1, Peters, 1991)
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and blanketing the regional unconformity truncating the peripheral parts of the Arabian-Nubian
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Shield (Johnson et al., 2011, 2013). Fig. 1 demonstrates just discontinuous outcrops of the entire
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Paleozoic sequence, whereas the actual immense extension, particularly of the lower Paleozoic
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siliciclastic sheet covers completely the northern margin of Gondwana as revealed by the
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subsurface maps (Petters, 1991; Alsharhan and Nairn, 1997).
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The invoked siliciclastic system in Jordan consists of an uppermost Ediacaran series,
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lower Paleozoic succession (Cambrian and Ordovician Systems, and lower Silurian
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Series=Llandovery), and Lower Cretaceous Series.
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Uppermost Ediacaran Umm Ghaddah Formation rests non-conformably above upper
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Ediacaran Aheimir Volcanic Suite (Figs. 3, 4A, 5A), or Sarmuj Conglomerate (Fig. 5A) or
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Hayala Volcaniclastic Formations, and is unconformably overlain by Fortunian Salab Formation.
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It consists of a rhyolitic monomictic conglomerate facies (facies A) and a sandstone facies
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(facies B) deposited by an alluvial fan and a braided river flowing northeastward (Table 1, Figs.
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2, 5A), respectively, and characterized by a large-scale fining upward succession that reflects the
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gradual cessation of the Pan African orogeny (Amireh et al., 2008).
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The Fortunian Salab sandstone starts non-conformably above the Neoproterozoic
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metamorphic, intrusive, and extrusive basement of the Aqaba (Fig. 4B) and the Araba
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Complexes. Predominant sandstones, with much less abundant conglomerates and silt-mudstones
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constitute the fluvial lower Cambrian Salab and the overlying Cambrian Umm Ishrin Formations
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(Figs. 4C, D). Both formations received detritus through braided rives flowing northward from
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the southerly located Arabian Shield (Table 1, Figs. 2, 5B, C; Amireh et al., 1994b). The lower
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part of the latter formation is replaced north-westley by shallow marine, well-sorted sandstone of
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the Abu Khusheiba Formation, which, in turn, is replaced further north-westley by carbonates,
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sandstones and mudstones of the Burj Formation (Amireh et al., 1994b). Trilobites and
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brachiopods yielding the late early Cambrian age, and rare occurrences of interbedded
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volcaniclastic conglomerates and volcanic tuffs (Fig. 4F) characterize the latter formation. The
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Ordovician System is more marine-influenced and consists mainly of sandstones with minor silt-
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mudstones, but lacks the carbonates. Fluvial sandstones of the lower Disi Formation
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conformably overlie the Umm Ishrin clastics. The transport direction of the braided rivers is
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similar to that of the underlying fluvial formations, which is northward (Table 1, Figs. 2, 5C;
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Amireh et al., 2001). Four siltstone-fine sandstone units characterized by Cruziana species and
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other ichnofossils interrupt this fluvial sequence (Bender, 1968; Amireh et al., 2001). The second
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Umm Saham Formation, overlying the Disi Formation, consists of a sandy fluvial-dominated
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lower part having the same northward dispersal direction, (Table 1, Figs. 2, 5C; Amireh et al.,
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2001) and a finer clastic upper part deposited in an intertidal environment (Amireh, et al., 2001).
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A deeper marine environment replaced the intertidal conditions during deposition of the third
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overlying Hiswa Formation (Fig. 5D). It consists of lower fine sandstone with interbedded
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mudstones carrying graptolites and deposited in a deeper environment, the lower shoreface to
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offshore, that grades upwards into mid shelf storm deposits (Makhlouf, 1988) then into the
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shallower upper shoreface environment. The fourth Dubaydib Formation consists of fine to very
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fine sandstone facies alternating with siltstone facies, and was deposited within the upper to
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lower shoreface zone but affected by three storm events (Figs. 4E, 5D; Amireh, et al., 2001).
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Fluctuations between the upper-lower shoreface and the open marine offshore conditions
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persisted through deposition of the overlying Tubailiyat, Batra, and Ratya Members of the fifth
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Mudawwara Formation, as well as the conformably overlying Llandovery Khusha Formation
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(Fig. 5D). Various types of ichnofossils are pervasive throughout the last four marine formations.
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The remaining parts of the Silurian System as well as the Devonian and the
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Carboniferous Systems are missing from the stratigraphy of Jordan (Bender, 1968). Most
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probably, they were truncated through the Hercynian orogeny (Saint-Marc, 1978) that affected
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the region during the Carboniferous, as indicated by their presence in adjoining countries
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(Husseini, 1989, 2000).
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The Triassic and Jurassic Systems are mainly non-clastic deposits, thus are not studied.
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The Lower Cretaceous Kurnub Group in northern Jordan consists of the Ramel, the Jarash, and
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the Bir Fa‘as Formations composed mainly of fluvial sandstone, some siltstone and
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conglomerate with few interbedded shallow marine arenaceous dolostone-limestone units
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(Amireh, 1997; Amireh and Abed, 1999). In central and south Jordan, the Kurnub Group consists
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of the Karak and Hammamat Formations composed entirely of terrestrial sandstone, and
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overlying the Bir Fa‘as Formation consisting of shallow marine sandstone and carbonate
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(Amireh, 2000). The transport direction of the braided to low sinuosity meandering rivers is
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persistently from the south-located Arabian Shield provenance towards the north and northwest-
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located Neo-Tethys (Table 1, Figs. 2, 5E; Amireh, 1993: 1997; 2000, Amireh and Abed, 1999).
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The Upper Cretaceous Series is composed of carbonates, evaporites, cherts, oil shales and
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phosphorites of the Ajlun and the Belqa Groups (Fig. 3).
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3. Tectonic and depositional environment development
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The uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan, the lower part of
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which constitutes a segment of the immense lower Paleozoic siliciclastic sheet blanketing most
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of the northern Gondwana margin and extending now from Arabia westward across north Africa
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to northwest and west Africa (Fig. 1, Peters, 1991). The Jordanian lower Paleozoic siliciclastic
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sequence received detrital sediment influx constantly from the Arabian-Nubian Shield, whereas
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the Mesozoic sequence received detritus additionally from the Paleozoic platform strata. The
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transport direction through braided rivers persisted from the south-located provenance towards
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the north and northwest located-Paleo and Neo-Tethys (Fig. 2). Following is a summary of
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tectonic events involved in the genesis of the Arabian Shield, and the depositional environment
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development of these platform strata, which are partly demonstrated in Fig. 5 as a series of five
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tectono sedimentary block diagrams.
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From the Mesoproterozoic (ca 1200 Ma) until ca 950 Ma the Mozambique Ocean opened
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by rifting of the eastern margin of the African Craton, within the Rodinia supercontinent. This
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rifting was associated with sea floor spreading (Hoffman, 1999). Several continental microplates
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and island arcs were produced then collided and accreted during the time interval of ca 950–750
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Ma forming the Arabian Shield (Stoeser and Camp, 1985; Al Shanti, 2009). Later on, the
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western part of the Arabian Shield collided with the African NE margin of Gondwana
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(Abdelsalam and Stern, 1996), closing the Mozambique Ocean and being welded to the northern
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part of the East African orogen (Hoffman, 1999), particularly the Saharan Metacraton (Fig. 1,
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Johnson et al., 2011). This thermo-tectonic activity is termed the Pan African orogeny (Kröner,
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1984). Afterwards, the western margin of the Arabian Shield collided with its central and eastern
198
parts, thus suturing the Arabian Shield with the African Continent between 640 and 620 Ma
199
(Husseini, 2000). This cratonization phase of accretionary and collisional (compressional)
200
tectonic processes and the complete assembly of the Arabian Shield gave rise to a new (Proto)
201
Arabian Craton (Al Shanti, 2009). An extensional collapse phase accompanied by deposition in
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202
syn-rift basins replaced the compressional phase during the time interval between 630 and 530
203
Ma (Husseini, 1989, 2000; Abdelsalam and Stern, 1996). Intrusions of postorogenic alkali rich
204
granites and rhyolites (Jarrar et al., 2008) dominated this extensional phase. The extensional
205
collapse of the Proto Arabian Craton witnessed the development of the regionally extensive Najd
206
Fault System and its complimentary syn-rift, down block-faulted, extensional basins (Fig. 5A)
207
with associated alkali rich granites and rhyolites (Jarrar, et al., 2003; Powell et al., 2015). The
208
Najd faults were active between about 630 Ma and 555 Ma (Johnson and Kattan, 2012), and
209
ceased gradually after that to end completely at about 530 Ma, prior to deposition of the
210
Cambrian sandstones over a vast peneplain situated at the eastern, northern, and northwestern
211
edge of the Arabian Shield (Johnson, et al., 2011).
212
Following the extensional rifting phase, which terminates the Neoproterozoic
213
amalgamation of northern Gondwana, an isostatic uplift and the accompanying erosion of the
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Neoproterozoic Aqaba Complex (Arabian Shield) and the later, but more localized, Ediacaran
215
Araba Complex cropping out in Wadi Araba (Fig. 2) took place. This extensive erosional phase
216
of the Jordanian basement complex gave rise to a peneplain, called Rum Unconformity (Fig. 4B;
217
Powell et al., 2014). The latter constitutes a fraction of the regional unconformity truncating the
218
peripheral parts of the Arabian-Nubian Shield (Johnson et al., 2011, 2013). Terrestrial
219
sedimentation had overlain this unconformity surface during the early Cambrian (Fig. 5B). A
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regional transgression of the Paleo-Tethys affected Jordan in the late early to mid-Cambrian that
221
was responsible for deposition of the regional Burj carbonates (Amireh et al., 1994b; Powell et
222
al., 2014) and followed by regressive siliciclastics. Terrestrial conditions resumed through the
223
remaining part of the Cambrian and through the Early Ordovician (Fig. 5C). Subsequently,
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224
shallow marine conditions dominated the study area during the Middle and Late Ordovician as
225
being a stable subsiding shelf along the northeastern margin of Gondwana (Fig. 5D)
226
(McGillivray and Husseini, 1992). At the end of the Late Ordovician, polar glaciers expanded
227
across Gondwana and covered most of western Arabia, including Jordan (Abed et. al, 1993), as
228
well as North Africa (Beuf et al., 1966). In the early Silurian, the retreat of glaciers introduced an
229
abrupt sea level rise and deposition of marginal marine shales that covered most of Gondwana
230
shelf. Therefore, Jordan was part of the stable Arabian Craton at the northeastern passive margin
231
of Gondwana facing the southern margin of the Paleo-Tethys during the early to mid-Paleozoic.
232
Moreover, no orogenies are recorded in Jordan from the mid Cambrian to the late Devonian.
233
In the late Carboniferous, a thermo-tectonic orogeny caused a regional domal uplift;
234
called “Geanticline of Heletz” (Gvirtzman and Weissbrod, 1984) affected Jordan and extended
235
from Sinai north to the western Palmyrides. This regional uplift is probably a manifestation of
236
the Hercynian (or Variscan) orogeny that was caused by collision and welding of Gondwana
237
with Laurassia leading to assembly of the supercontinent Pangaea during the late Carboniferous.
238
The uplift was associated with rifting and magmatism and subjected to extensive erosion leading
239
to a significant hiatus in Jordan stripping away the Ordovician through the Devonian especially
240
in western Jordan, and giving rise to a NS strip-like configuration of the Cambrian and the
241
Ordovician outcrops in Jordan (Fig. 2).
242
In the late Permian and Triassic, the Turkish and Sanadaj-Sirjan area of the Cimmerian
243
Continent became separated from the Arabian Gondwana by the Zagros rift initiating the Neo-
244
Tethys (Şengör et al., 1988). During the Triassic (to Early Jurassic), an extensional phase
13
245
resulted due to continued rifting along the Zagros suture (Şengör et al., 1988) that extended and
246
stretched the Arabian plate, causing deep-seated normal faults. From the Early to the Late
247
Jurassic Arabia again entered a period of tectonic quiescence.
248
At the close up of the Jurassic, the lithospheric extension, continental rifting, and
249
associated uplift resumed in Arabia due to continuation of the breakup processes in Gondwana
250
(Guiraud and Maurin, 1992). The orogenic uplift of the block faulted continental crust was
251
accompanied by a deep erosional phase that truncated a great proportion of the Jurassic sequence
252
in Jordan (Bender, 1968; Bandel, 1981). This extensive erosion is indicated by presence of a
253
basal conglomerate lining the unconformity surface above the remaining Middle Jurassic
254
sequence (Amireh, 1997; Amireh and Abed, 1999). Gradually, and through the Early Cretaceous,
255
the tectonic uplift ceased in the region, and tectonic quiescence prevailed. Consequently, fluvial
256
sedimentation dominated in central and southern Jordan (Fig. 5E), whereas northern Jordan,
257
which is closer to the Neo-Tethys, was affected by several marine ingressions (Amireh, 1997;
258
Amireh and Abed, 1999). During the Late Cretaceous, Jordan within Arabia was widely
259
transgressed by the Neo-Tethys (Dercourt et al., 1993).
260
261
4. Arabian-Nubian Shield provenance
262
The paleocurrent directions determined through 1339 reliable measurements of planar
263
and trough cross bedding azimuths in the uppermost Ediacaran-Lower Cretaceous siliciclastic
264
sequence are summarized in Table 1 following Amireh (1993, 1997, 2000), Amireh and Abed
14
265
(1999), and Amireh et al. (1994b, 2001, 2008). In addition, these paleocurrents are portrayed on
266
the geological map of Jordan (Fig. 2), and demonstrated by the tectono sedimentary block
267
diagrams (Fig. 5). According to these paleocurrent dispersal directions, the southerly-located
268
Arabian-Nubian Shield (ANS) can be determined with a great significance to represent the
269
constant provenance for the siliciclastic sequence in Jordan throughout the late Ediacaran-Late
270
Cretaceous. In the Paleozoic Era, the detritus was shed from this southerly ANS provenance and
271
transported by braided rivers towards the north and northwest-located Paleo-Tethys (Bender,
272
1968; Schneider et al., 1984, 2007; Amireh, 1987, 1991, 1992, 1993; Amireh et al., 1994b, 2001;
273
Powell, 1989). In the Mesozoic Era, braided and low sinuosity meandering rivers, similarly,
274
transported siliciclastic sediments from this southerly ANS to the north and northwest-located
275
Neo-Tethys (Bender, 1968; Amireh, 1987, 1991, 1993, 1997, 2000; Amireh and Abed, 1999).
276
This northward dispersal direction from the southerly ANS towards the north and northwest-
277
located Paleo then Neo-Tethys during the Paleozoic and Mesozoic, respectively, is also well-
278
recorded in the adjacent countries (Weissbrod and Nachmias, 1986; Klitzsch and Squyres, 1990;
279
Alsharahn and Nairn, 1997; Garfunkle, 1999, 2002).
280
Moreover, this ANS provenance is recently confirmed through SHRIMP and SIMS U-Pb
281
geochronological dating of detrital zircon grains from these siliciclastic deposits (Kröner et al.,
282
1990, Stern et al., 1994; Wilde and Youssef, 2002; Avigad et al., 2003, 2015; Kolodner et al.,
283
2006; Samuel and Youssef, 2011; Morag et al., 2012; Yaseen et al. 2013; and Nasiri Bezenjani,
284
et al., 2014).
15
285
Yaseen et al. (2013) constrained ages ranging between 650 and 600 Ma in the Saramuj
286
Conglomerate Formation constituting part of the basement below the sequence under
287
investigation (Figs. 1, 2), and recorded the ANS to be the provenance, particularly the Aqaba
288
Complex now exposed in southern Jordan within the northernmost part of the ANS. Just west of
289
the study area, Kröner et al. (1990), Avigad et al. (2003, 2015, 2017), Kolodner et al. (2006), and
290
Morag et al. (2012) similarly recorded this Neoproterozoic ANS provenance for the Cambrian
291
and Ordovician siliciclastic sequence. Kröner et al. (1990) dated detrital zircon grains from
292
several rock types in Elat basement and in the adjacent Sinai (Fig. 1) to range from 820 to 800
293
Ma.
294
Avigad, et al. (2003) recorded a 550-650 Ma age of detrital zircon grains in Cambrian
295
unit in Elat area (Fig. 1) that indicates the calk alkaline and alkaline igneous rocks of the
296
Neoproterozoic ANS provenance. They documented, also, zircon grains yielding older ages, pre
297
Neoproterozoic that reach up to 2.7 Ga, which may indicate the Saharan Metacraton provenance,
298
or the southern Affif terrane in northwest Arabia (Fig. 1). Avigad et al. (2015) based on U-Pb-Hf
299
detrital zircon geochronology of the Zenifim Formation subcropping in Northern and Southern
300
Negev (Fig. 1) identified the granites of the adjacent ANS formed at the cessation of the
301
Neoproterozoic orogeny as a major provenance for these late Ediacaran arkoses.
302
Recently, Avigad et al. (2017) used detrital rutile U-Pb geochronology to deduce a broad North
303
African source for the Cambro-Ordovician sandstone cropping out in Elat area (Fig. 1), southern
304
Jordan, and Ethiopia.
16
305
Kolodner et al. (2006) constrained a U-Pb (900-530 Ma) age indicating derivation of the
306
Cambrian and Ordovician siliciclastics from the proximal northern part of the Arabian-Nubian
307
Shield. They attributed older ages that reach up to 2.7 Ga, to be derived from a more distal
308
southern provenance, such as the northern parts of the Tanzanian-Congo (Fig. 1) and the
309
Dhrawer Cratons, or a western provenance such as the Western Desert, or the Gebel Oweinat
310
area (Fig. 1). Kolodner et al. (2009) also investigated the detrital zircon U-Pb in Lower
311
Cretaceous sandstone cropping out in Northern Negev (Fig. 1), and Elat region (Fig. 1), and
312
concluded that they are mostly derived from reworking of the Paleozoic section. Morag et al.
313
(2012) documented a northern ANS as a provenance to the Elat conglomerate unit (Fig. 1) based
314
on detrital zircon grains ranging in age from 1.0 Ga to around 580 Ma.
315
Westward, at southern Sinai (Fig. 1), Samuel et al. (2011) constrained the age of the
316
Rutig conglomerate between 850 and 600 Ma, concluded the provenance to be the ANS material
317
in Sinai, and confined deposition of different levels of the conglomerates to ca 620–610 Ma and
318
600–590 Ma.
319
Farther westward, Wilde and Youssef (2002) constrained the age of the sedimentary
320
Hammamat Group in the North Eastern Desert (Fig. 1), to be 585 ± 13 Ma, and concluded that
321
the zircon grains were derived from the adjacent Dokhan Volcanic Series. In addition, they
322
recorded older ages, up to ca 2630 Ma, indicating contributions from Proterozoic and Archean
323
sources that may lie in the Central and South Eastern Desert (Fig. 1), the Nile Craton, or in a
324
remote part of the ANS.
17
325
Southwestward of study area, Stern et al. (1994) dated conglomerates and other
326
metamorphic and igneous rocks of the Precambrian basement around Wadi Halfa (Fig. 1), to
327
range from 2.6 to 0.72 Ga, and concluded that the conglomerate is derived from a local source.
328 329
Southward of study area, the age of Talbah Group in the Midyan terrane of NW Arabia
330
(Fig. 1) is constrained by Nasiri Bezenjani, et al. (2014) to range from 635 ± 5 Ma to 569 ± 10
331
Ma. They recorded also that it derived detritus from the Central Eastern Desert and Midyan
332
terrane island arc basement for its lower and middle parts, and from other parts of the ANS for
333
its upper part. In the same region, detrital zircon grains from tuff beds in the Dhaiqa and Rubtayn
334
basins within the Jibalah Group (Fig. 1) yields SIMS U-Pb ages suggesting deposition between
335
600 and 570 Ma (Kennedy et al., 2011).
336
337
5. Methods and terminology
338
The bulk petrographic compositional approach is applied in the present study. Three hundred
339
forty one fresh siliciclastic sandstone samples were collected from 19 profiles across the
340
outcrops of the uppermost Ediacaran-Lower Cretaceous clastic sequence, and from oil
341
exploration wells HM-2, AJ-1, NH-1, and WS-3 in Jordan (Fig. 2). The outcrop and well-core
342
sandstones are mainly medium to coarse-grained leading to reliable identification and favorable
343
counting results. The sandstone samples were thin-sectioned after epoxy impregnation for the
344
semi indurate or slightly friable samples. Subsequently, they were examined by the routine
345
polarized light microscope. About 500 points were counted in each thin section to determine the
18
346
modes of the detrital framework grains, the detrital matrix and the cements. Counting errors for
347
the grain parameters are less than 5% of the whole rock for individual counts.
348
Gazzi-Dickinson point counting method (Ingersoll et al., 1984) that minimizes the
349
dependence of composition on grain size is employed to achieve reliable results (Gazzi, 1966;
350
Dickinson, 1970; Ingersoll, 2012). Moreover, all sandstone samples employed for point counting
351
have intact framework grains not affected by diagenesis, particularly intrastratal solution and
352
replacement as indicated by having a matrix and/or a cement generally not exceeding 25% that
353
would otherwise both affect or alter the framework constituents (cf. Dickinson and Suczek,
354
1979; Dickinson et al., 1983). Additionally, the matrix and the cements just fill passively the
355
interstitial spaces between the framework grains, not altering them, and thus leading to reliable
356
identification.
357
The framework modes of quartz, feldspar and lithic fragments are recalculated to 100%
358
in order to determine the type of the sandstone applying a modified classification of Pettijohn et
359
al. (1987; Fig. 6). The modifications represent an addition of a prefix to the class of the
360
sandstone expressing a characteristic component not appearing in the classification, and
361
subdivision of the arkose field into arkosic arenite and lithic arkosic arenite subfields, as well as
362
subdivision of the lithic arenite field into feldspathic litharenite and litharenite subfields.
363
The variants of quartz, feldspar, and lithic fragments are recalculated to the various
364
petrographic parameters to be plotted in the triangular compositional diagrams of Dickinson and
365
Suczek (1979) and Dickinson et al. (1983).
19
366
367
6. Results
368
The mean, standard deviation, and confidence level of 95% for the sandstone component
369
parameters obtained for each member, formation, or group are listed in Table 2 and Appendix A.
370
The means of the framework modes for most of the formations have standard deviations
371
(STDEV. S) less than 10%, and rarely 10 to 15% of the whole rock (Table 2). Such values of
372
standard deviations of means imply that the formations are petrographically homogenous. The
373
“P” values of confidence level 95% calculated for the formations (Table 2; Appendix A),
374
excluding the null hypothesis value or empty set having no elements in the set, are mainly less
375
than the significance (alpha) level of 0.05, thus indicating the statistical significance of the
376
various component parameters (hypothesis test).
377
The sandstone components parameters include the modes of: framework grains (FW,
378
Figs. 7-9), detrital matrix (Mt, Fig. 7A), cements (C, Figs. 7B-E), total quartz (Qt), total feldspar
379
(F), lithic fragments (L), monocrystalline quartz (Qm), polycrystalline quartz (Qp), total lithic
380
fragments (Lt), volcanic lithic fragments (Lv), sedimentary/metasedimentary lithic fragments
381
(Ls), plagioclase (P), and K-feldspar (K).
382
Qt equals the sum of Qm (Figs. 7B, D, E, F) and Qp (Figs. 8A, B), whereas F represents
383
the sum of K-feldspar (mainly orthoclase, Fig. 8E, and less commonly microcline, Fig. 8F) and
384
plagioclase. L equals the sum of Lv (Figs. 8C, D, 9A-E) and Ls (Figs. 10A-D), whereas Lt
385
represents the sum of L and Qp.
20
386
Triangular QtFL, QmFLt, QpLvLs, and QmPK compositional diagrams following
387
Dickinson and Suczek (1979) and Dickinson et al. (1983) are constructed for the mean
388
framework modes for all the members, formations, or groups of the investigated sequence (Fig.
389
11). Moreover, representation of all individual samples on these compositional diagrams is
390
available at the link: http://link-placeholder.com .
391
Based upon the total quartz (Qt), total feldspar (F) and lithic fragments (L) parameters for the
392
members, formations or groups investigated, the types of sandstone are determined applying the
393
modified classification of Pettijhon et al., (1987) (Fig. 6).
394
395
7. Discussion
396
The uppermost Ediacaran-Lower Cretaceous clastic sequence under investigation can be split
397
into five sandstone suites. Each one consists of a group of sandstone samples that are closely
398
related both spatially and stratigraphically (cf., Dickinson et al., 1983) and having same
399
sandstone type. The individual sandstone suite represents either one formation or several
400
associated formations, for each of which the common framework modes, might indicate
401
derivation from a specific provenance terrane, thus represents mainly, a relatively unchanged
402
plate tectonic setting. However, interpretation of the detrital framework modes is based upon the
403
individual formations rather than the sandstone suites. From other point of view, this
404
interpretation of modal composition is based upon comparison with present-day plate tectonic
405
processes that probably were different during the Paleozoic and Mesozoic, and particularly
21
406
during the late Ediacaran. However, Dickinson‘s plate tectonic provenance approach is
407
established mainly upon Paleozoic and Mesozoic, and some late Precambrian sandstone suites
408
(sandstone suites numbers 10, 11 and 25, Dickinson and Suczek, 1979; latest Precambrian to mid
409
Ordovician sandstone suite, Dickinson, et al., 1983).
410
411
7.1. Sandstone suite number 1: Umm Ghaddah Formation of late Ediacaran-early Cambrian age
412
Umm Ghaddah Formation consists of a conglomerate facies and a sandstone facies. The detrital
413
framework modes of the sandy matrix of the conglomerates and the sandstones is composed
414
mainly of monocrystalline and polycrystalline quartz, K-feldspar, rhyolitic rock fragments,
415
subordinate plagioclase and rare sedimentary and metamorphic lithic fragments (Table 2).
416
According to the means of the Qt, F, and R (L) parameters (Table 2), the sandstone is classified
417
as a rhyolitic litharenite (Fig. 6).
418
It can be seen from the QtFL compositional diagram (Fig. 11A) that the means of these
419
parameters fall within the recycled orogenic provenance field. The QmFLt plot (Fig. 11B)
420
augments this inference, and specifies it to be the transitional recycled orogenic provenance.
421
According to the QpLvLs and QmPK compositional diagrams (Figs. 11C, D), the provenance
422
terrane can be inferred to be the magmatic arc orogen, and the continental block or the recycled
423
orogenic terrane, respectively. Which one of these inferences is true? An attempt to answer this
424
question will follow integrating the achieved petrographic results, together with the tectonic,
22
425
geologic, sedimentological, and climatological data presented in the section of tectonic and
426
depositional environment development.
427
Umm Ghaddah Formation has an age ranging from the late Ediacaran to the early
428
Cambrian (Amireh, et al., 2008). This age could be constrained between 598.2 ± 3.8 Ma, the age
429
of the underlying Aheimir Volcanic Suite (Jarrar et al., 2012), and tentatively 541 Ma (Fortunian
430
Age, Cohen et al., 2016), the age of the overlying Salab Formation dated by Amireh et al.
431
(1994b) according to the presence of Cruziana aegyptica ichnofossil. At this time span, the
432
Arabian Shield provenance has already been stabilized or cratonized into the stable craton “Proto
433
Arabian Craton” devoid of collisional-accretional magmatic arcs processes that ceased at about
434
630 Ma (Al Shanti, 2009), thus before deposition of the present formation.
435
Moreover, the magmatic arc provenance terrane can be refuted according to the following
436
petrographic criteria. 1) The rarity of plagioclase (Table 2), since the sands derived from most
437
magmatic arcs are commonly enriched with plagioclase or, are characterized by a high ratio of
438
plagioclase to K-feldspar (Dickinson 1985; Ingersoll, 2012). 2) The quartz content is higher here
439
than that of typical magmatic arc terranes (Dickinson and Suczek, 1979). 3) The types of the
440
lithic fragments being mainly acidic rhyolitic (Figs. 8C, D, 9A-E) rather than intermediate
441
andesitic or basic basaltic (Fig. 9F) as the sands derived from most magmatic arcs of
442
intermediate-composition (Dickinson, 1985; Marsaglia and Ingersoll, 1992; Ingersoll, 2012).
443
These rhyolitic lithic fragments were derived mainly from a local provenance; upper Ediacaran
444
Aheimir Volcanic Suite, cropping out in central part of Wadi Araba (Fig. 2), and not related
23
445
genetically to any island arc but represents an intracratonic syn-rift volcanic extrusion (Jarrar,
446
1992; Jarrar et al., 1992).
447
Regarding the inferred recycled orogenic provenance, the subduction complexes of
448
deformed oceanic sediments and lavas can be excluded based on the absence or rarity of clasts
449
indicating shedding from ophiolites and oceanic crust, or from other sedimentary source, such as
450
greenstone, chert (Figs. 8C, D, 8A, E), shale, argillite, slate, phyllite, greywacke and limestone
451
(Dickinson and Suczek , 1979; Dickinson, 1985). The recycled collisional orogenic and the
452
foreland uplifts associated with foreland fold thrust belts provenance types can be also ruled out
453
according to the rarity of sedimentary (Figs. 10A, B) and metasedimentary lithic fragments (Figs.
454
10C, D), and absence of criteria indicative of recycling, such as two stages of syntaxial quartz
455
overgrowths.
456
This erroneous magmatic arc and recycled orogenic provenance terranes interpretation
457
employing Dickinson‘s petrographic model might be attributed to the high mode of the rhyolitic
458
lithic fragments (Table 2). They were contributed from the local, post-orogenic Aheimir
459
intracratonic syn-rift extrusion, where the plate tectonic setting of these rift-related volcanic
460
rocks are not represented by Dickinson‘s Plate tectonics-provenance diagrams. They cause
461
pulling of the means of the QtFL, QmFLt parameters to fall in the erroneous recycled orogenic,
462
and transitional recycled orogenic provenance fields, respectively, departing probably from the
463
more appropriate basement uplift continental block field. Furthermore, they also cause the means
464
of the QpLvLs parameters to fall erroneously close to the Lv pole in the magmatic arc
465
provenance field. Consequently, in order to interpret the detrital framework modes, the proposed
24
466
provenance terrane, as well as the other sedimentological and climatological factors should be
467
evaluated.
468
At the late Ediacaran-early Cambrian the study area underwent the final extensional
469
rifting phase of the Pan African orogeny (Jarrar et al., 1991) that caused block faulting of the
470
Arabian Shield leading to development of a series of half-grabens, grabens and horsts, or
471
generally local uplifted basement blocks (Fig. 5A). Therefore, a basement uplift provenance
472
terrane of the NE Gondwana continental block seems to be the most appropriate one. Amireh et
473
al. (2008) recorded that Umm Ghaddah Formation was deposited in intracratonic rift system
474
basins bounded by active listric half-graben faults (Fig. 5A). Their uplifted shoulders,
475
particularly the footwall upland, and the hangingwall lowland source rocks, as well as the
476
intrabasinal horst structures were subjected to a high rate of erosion. Consequently, coarse
477
gravelly detritus was shed and rapidly deposited in the intracratonic basins as transverse alluvial
478
fans, whereas the sandy debris was deposited as a proximal axial braidplain (Fig. 5A). The
479
source rocks were the granitoids and gneisses of the Aqaba and the Araba Complexes of the
480
Arabian Shield, and the local Aheimir Volcanic Suite (Figs. 2, 5A). The latter source rocks
481
contributed the gravely debris to the adjacent intermontane rift basins as those depicted in
482
profiles number 12 and 13 (Fig. 2; Amireh et al., 2008), and the sand to the further rift basins as
483
those represented in profile number 16 and in HM-2, WS-3, AJ-1, and NH-3 wells (Fig. 2;
484
Amireh et al., 2008). On the other hand, the monocrystalline and polycrystalline quartz, K-
485
feldspar, and plagioclase grains were delivered to all the intermontane rift basins from the
486
Arabian Shield, where its northern flank crops out in southwestern Jordan (Fig. 2), as discussed
487
in section 3.
25
488
The source rocks and the released detritus were subjected to an intense chemical
489
weathering due to the prevailing hot humid climate (Wolfart, 1981, Konert et al., 2001, Amireh
490
et al., 2008). Under these conditions of active tectonic uplift, high relief, high rate of erosion,
491
very short transport distance, and rapid sedimentation in proximal alluvial fans and braidplains
492
within the adjacent intermontane rift basins, a great proportion of the rhyolitic lithic fragments
493
(L= 44.4%, mainly Lv, Table 2) could escape the intense chemical weathering. On the other
494
hand, through the longer transport distance of the sandy detritus from the Aqaba and the Araba
495
Complexes, and probably from other southern parts of the Arabian Shield, to the depositional
496
intermontane rift basins (Fig. 2), the intense chemical weathering as well as the mechanical
497
weathering could dissolve and destruct a large proportion of the unstable feldspars. The survived
498
remnants, mainly K-feldspar and rarely plagioclase (F= 12.6%, Table 2), together with the stable
499
quartz varieties (Qt= 43.0%), and the rhyolitic lithic fragments managed to arrive safely to the
500
depositional intermontane rift basins, and to give rise ultimately to the immature rhyolitic
501
litharenites.
502
503
7.2. Sandstone suite number 2: Salab, Burj and Abu Khusheiba Formations of early to mid-
504
Cambrian age
505
Sandstone suite number 2 consists of the lower Cambrian Salab, the overlying lower-middle
506
Cambrian Burj, and the coeval Abu Khusheiba Formations. The Salab Formation has a
507
subarkosic arenite composition (F= 17.2%, Table 2; Figs. 8E, F) and the Abu Khusheiba
508
Formation is also composed of subarkosic arenite but with a lower feldspar mode (F=11%, Table
26
509
2). On the other hand, the Burj Formation has a rhyolitic sublitharenite composition (F= 7.5%,
510
L= 20%, Table 2).
511
It can be seen from QtFL compositional diagram (Fig. 11A) that the means of these
512
parameters for the Salab, Abu Khusheiba, and Burj Formations fall in the transitional continental
513
block, craton interior continental block, and recycled orogenic provenance terranes, respectively.
514
The QmFLt plot (Fig. 11B) augments the inference for the Salab and Abu Khusheiba
515
Formations, and specifies the provenance terrane for the Burj Formation to be the quartzose
516
recycled orogen. Upon employing the QpLvLs compositional diagram (Fig. 11C); the means of
517
these parameters for the Burj Formation fall in the mixed orogenic provenance terrane
518
contradicting with those derived from the QtFL and QmFLt plots. On the other hand, plotting
519
means of the QmPK parameters for the three formations (Fig. 11D) yields a better result, where
520
all of them are located close to the Qm pole indicating an increasing maturity or stability of
521
detritus derived from the continental block provenance terranes (Dickinson and Suczek, 1979).
522
In contrast to the Lv parameter, the P, and K parameters of the three formations are both
523
petrographically homogenous and statistically significant (Table 2).
524
The transitional continental block and the craton interior continental block provenance
525
terranes inferred for the Salab and the Abu Khusheiba Formations, respectively, fit very well
526
with the petrographic and the other data documented here. Therefore, the modal framework
527
composition of both formations can be fully interpreted based upon these inferred provenance
528
terranes together with the influence of the other secondary factors.
27
529
The last extensional rifting phase of the Pan African orogeny started to cease gradually
530
from the late Ediacaran (cf. Husseini, 1989; Abdelsalam and Stern, 1996; Jarrar et al., 2003;
531
Amireh et al., 2008), so that at the early Cambrian, a much-reduced tectonic uplift prevailed, less
532
than that of Umm Ghaddah Formation. Consequently, the continental block was less affected by
533
the block faulting processes leading to a reduced basement uplift. The plate tectonic setting of
534
the continental block corresponds most probably to the transitional provenance terrane.
535
Therefore, a moderate relief characterized the Arabian Shield source rocks; intermediate between
536
the high relief of the basement uplifts and the low relief of the craton interior. This moderate
537
relief also characterized the rhyolite paleohigh that existed in Wadi Abu Khusheiba area, central
538
Wadi Araba (Abed, 2000), which was probably a broad positive topography rather than a strong
539
local relief as those produced by the block-faulting phase of the Pan Africa orogeny and
540
characterized the Umm Ghaddah Formation. This moderate relief was in turn responsible for a
541
moderate rate of erosion. Under the persisting hot humid climate, the intensive chemical
542
weathering continued affecting the granitoids and the gneissic source rocks and the sandy
543
detritus consisting of unstable feldspars and rhyolitic lithic fragments, and the stable quartz
544
varieties. However, the sediments were transported relatively a short distance by braided rivers,
545
and rapidly deposited in sand flats of the proximal-medial braidplains (Profiles number 1 and 14,
546
Fig. 2; Amireh et al., 1994b). Such conditions gave a chance to a great proportion of the unstable
547
feldspar grains (F= 17.2%, Table 2) to escape the intense chemical weathering and the
548
mechanical weathering during transit, and to reach the fluvial depositional environment. These
549
feldspars together with the stable quartz gave rise ultimately to the immature subarkosic arenites
550
of the Salab Formation.
28
551
The lower mode of feldspars of the overlying Abu Khusheiba Formation (F= 11.0%,
552
Table 2) can be attributed to the lower relief of the inferred craton interior provenance terrane
553
due to the almost complete cease of the Pan African orogeny. Consequently, the low relief
554
contributed feldspar grains at a retarded rate of erosion, which were severely affected by the
555
prevailing chemical weathering. Moreover, the feldspars were also partially destructed by the
556
mechanical attrition in the more energetic beach depositional environment of the Abu Khusheiba
557
Formation (Amireh, 1987; Amireh et al., 1994b).
558
The inferred quartzose recycled orogenic provenance terrane of the Burj Formation
559
seems to be erroneous according to the absence of the petrographic evidence indicating
560
reworking from the stratal source rocks, such as a high mode of sedimentary or metamorphic
561
lithic clasts, where Ls attains only 4.1% (Table 2), or presence of two stages of quartz
562
overgrowths. Additionally, no folded strata or thrust belts are recorded in the Arabian Craton
563
source rocks as discussed in the tectonic and depositional environment development section.
564
Moreover, the high modes of the rhyolitic lithic fragments (L= 22.0%, Lv= 61.9%, Table 2)
565
derived from the local sources cause pulling of the means of the QmFL parameters to fall in the
566
quartzose recycled orogenic provenance subfield departing from the more appropriate craton
567
interior provenance terrane of the continental block. Additionally, the latter provenance terrane is
568
implied upon comparison with that of the covalent Abu Khusheiba Formation, where almost
569
similar conditions prevailed. However, the higher rhyolitic lithic fragments mode in the Burj
570
Formation could be attributed to the influence of a nearby local rhyolitic extrusion, located
571
north-westley of Wadi Araba (Fig. 2), and formed during the last postorogenic volcanism of the
29
572
extensional rifting phase of the Pan African orogeny that might lasted sometime in the Cambrian
573
(Beyth and Heimann, 1999).
574
This volcanic activity, which was blanketed by the succeeding fluvial siliciclastics of
575
Umm Ishrin Formation, is rather different from the older, more voluminous Neoproterozoic
576
Aheimir Volcanic suite that configured paleohighs at time of deposition of the Abu Khusheiba
577
Formation, and the coeval Burj Formation. Position of this postulated volcanic extrusion is
578
indicated here from the systematic southeastward decrease of the rhyolitic lithic fragments
579
modes in the three lateral covalent Burj, Abu Khusheiba, and the lower part of the Umm Ishrin
580
Formation, where they attain 22.0%, 1.8%, and 0.3%, respectively (Table 2). Figure 4F shows a
581
volcaniclastic conglomerate bed and a volcanic ash layer, among others recorded by Amireh
582
(1987), interbedded in the Burj Formation that could also indicate such volcanic source.
583
According to these volcaniclastic conglomerate and the volcanic ash layer Amireh (1987, p. 13)
584
recorded the presence of a “nearby volcanic activity”.
585
From other point of view, it should be stated here, that this proposed volcanic activity
586
delivered volcanic detritus to the depositional site with a variable rate through the time of the
587
Burj Formation, where Lv mode ranges from 0 to 63 (Appendix A.3). This variable rate of
588
volcanic flux is responsible for the high standard deviation of the Lv parameter recorded in the
589
Burj Formation that attains 31.6% (Table 2, Appendix A.3).
590
Moreover, the presence of devitrified volcaniclasts exhibiting original glassy textures, and
591
devitrified feldspar and pyroclastic phenocrysts (Figs. 9C, D) might substantiate the existence of
592
this volcanic activity. Additionally, the occurrence of barite cement (Amireh, 1987, 1991), and
30
593
apatite overgrowth (Fig. 8F), which are diagenetic processes indicative of volcanic-hydrothermal
594
activities (Bentz and Martini, 1968; Ramdohr, 1975) could further confirm the invoked volcanic
595
activity. It can be argued, that the apatite overgrowth results from the lower-middle Cambrian
596
major worldwide episode of phosphorite formation (Brasier and Callow, 2007). This argument
597
can be disregarded since this apatite overgrowth occurs in the lower part of the fluvial Umm
598
Ishrin Formation, which surely was not affected by this marine phosphorite depositional event.
599
600
7.3. Sandstone suite number 3: Umm Ishrin, Disi and Umm Saham Formations of mid-
601
Cambrian to Mid-Ordovician age
602
Sandstone suite number 3 consists of the middle-upper Cambrian Umm Ishrin, the upper
603
Cambrian-Lower Ordovician Disi, and the Lower Ordovician Umm Saham Formations that were
604
deposited by braided rivers on the southern stable shelf of the Paleo-Tethys flanking the Arabian
605
Shield. This sandstone suite is composed entirely of super mature quartzarenites (Fig. 6) devoid
606
of any single feldspar grain. Invariably, the QtFL compositional diagram (Fig. 11A) exhibits the
607
craton interior of the continental block as the sole provenance terrane for the three formations.
608
Additionally, the QmFLt compositional diagram (Fig. 11B) augments this result for the Umm
609
Saham Formation, and displays the Umm Ishrin and the Disi Formations to fall at the boundary
610
between the craton interior and the quartzose recycled orogenic provenance subfields. The
611
QpLvLs and QmPK compositional diagrams (Figs. 11C, D) have no significance, since the
612
modes of these parameters for the three formations are either zero or very low (Table 2). This is
613
normally the case for the craton interior sandstone suites (Dickinson and Suczek, 1979).
31
614
The inferred craton interior provenance terrane of the continental block fits very well
615
with the achieved petrographic data and observations. However, the influence of the other factors
616
should be also assessed. The granitoids and gneisses of the Arabian Shield consistently supplied
617
sandy detritus to the present sandstone suite in a similar way to the previous ones. The
618
siliciclastic debris included the two varieties of quartz, feldspars, and rhyolitic rock fragments.
619
At the mid-Cambrian to Mid-Ordovician time, no orogenic activity has been recorded in the
620
study area. Consequently, the source rocks were characterized by a broad positive low relief
621
leading to a retarded rate of erosion. Intense chemical weathering under the persisting warm
622
humid climate affected the source rocks with the low gradients, as well as the slowly released
623
sandy detritus that were further transported a long distance by braided rivers across continental
624
surfaces having low gradients to the distal braidplains (Amireh et al., 1994b; Amireh et al.,
625
2001). The sediments that resided a certain time on bar tops and at overbanks were also affected
626
by this vigorous chemical weathering. Moreover, mechanical weathering, causing destruction
627
along cleavage planes and leading to grains disintegration, certainly affected the mechanically
628
unstable feldspars during this prolonged fluvial transport. Under such conditions of active
629
chemical and physical weathering, all the unstable feldspars and rhyolitic rock fragments were
630
totally dissolved or destructed, whereas the more stable quartz survived, thus giving rise
631
ultimately to the super mature first-cycle quartzarenite. Such a super mature first-cycle
632
quartzarenite is recorded in various cases formed under similar conditions (Van Andel, 1959;
633
Pettijohn, 1975; Mack, 1984, Dickinson, 1985; Garzanti et al., 2013).
634
32
635
7.4. Sandstone suite number 4: Hiswa, Dubaydib, Mudawwara, and Khusha Formations of Early
636
Ordovician to early Silurian age
637
Sandstone suite number 4 consisting of Lower Ordovician Hiswa, Middle-Upper Ordovician
638
Dubaydib, Upper Ordovician-lower Silurian Mudawwara, and lower Silurian Khusha Formations
639
has invariably a subarkosic arenite composition (Fig. 6, Table 2). The depositional environment
640
is marine, fluctuating between the intertidal-subtiadal, and the deep offshore zones.
641
It can be seen from the QtFL and QmFLt compositional diagrams (Figs. 11A, B) that the
642
means of these parameters for the Hiswa Formation fall in the craton interior continental block
643
provenance field, whereas they fall in the transitional continental block provenance field for the
644
Dubaydib, the Mudawwara and the Khusha Formations. The inferred transitional continental
645
block provenance terrane seems to be erroneous. This is because it implies a moderate relief of
646
the Arabian Shield source rocks that in turn indicates a moderate tectonic uplift, which is not
647
correct since the study area underwent a tectonic quiescence between the mid Cambrian and the
648
early Carboniferous. Consequently, the relief of the Arabian Shield should be low, thus a stable
649
craton interior provenance terrane of the continental block might be indicated, which is already
650
the provenance type inferred for the underlying Hiswa Formation of the same sandstone suite.
651
Moreover, it could represent a continuation of the provenance terrane for the preceding
652
sandstone suite, which was similarly deposited under the same tectonic quiescence. How can the
653
framework modes of the present sandstone suite (Table 2) be interpreted in terms of this
654
indicated craton interior provenance terrane?
33
655
The granitiods and gneissic source rocks of this stable craton interior with the
656
characteristic low relief contributed the necessary feldspars that managed somehow to reach the
657
marine depositional environment. Although the rate of erosion was low, the released unstable
658
feldspar grains were not attacked or dissolved neither at the source rocks nor through transit.
659
This is attributed to the absence of chemical weathering during deposition of the present
660
sandstone suite, which, on the contrary, persisted during the time of all the preceding sandstone
661
suites. The reason beyond that is the cold arid or semiarid climate prevailing under the well-
662
known Late Ordovician glacial event that affected the study area within northeast Gondwana
663
(Abed et al., 1993), hens the acting weathering was mechanical rather than chemical. Moreover,
664
the feldspar grains were transported a very short distance by braided rivers to the adjacent
665
shallow marine depositional basin (see position of profiles (outcrops) number 5-11 that are very
666
close to the Arabian Shield, Fig. 2), thus they were not destroyed mechanically. Additionally, the
667
marine environment was gentle or mild on these labile feldspars. Under these conditions of
668
complete absence of chemical weathering and insignificant mechanical weathering, the unstable
669
feldspars, besides the stable quartz gave rise ultimately to the immature subarkosic arenites of
670
the sandstone suite.
671
It can be concluded here, that the erroneous inference of the transitional provenance
672
terrane of the continental block for the Dubaydib, the Mudawwara, and the Khusha Formations
673
applying Dickinson‘s plate tectonic-provenance approach is attributed to the rather unusual
674
influence of the glacial paleo climate.
675
34
676
7.5. Sandstone suite number 5: Kurnub Group of Early Cretaceous age
677
Sandstone suite number 5 consists of the Lower Cretaceous Kurnub Group, and is remarkably
678
composed of a mature quartzarenite (Table 2, Fig. 6). Both of the QtFL and QmFLt
679
compositional diagrams display unequivocal craton interior provenance terrane of the continental
680
block (Figs. 11A, B). This inferred provenance terrane fits very well with the petrographic data
681
and observations recorded here. The detrital framework modes consist almost totally of the two
682
quartz varieties (Qt= 99.7%, Table 2), with a very low feldspar mode (F= 0.3%, Table 2), and
683
can be satisfactorily attributed to the inferred craton interior provenance terrane in hand with the
684
other secondary factors.
685
Similar to the previous four sandstone suites, the provenance terrane is the Arabian
686
Shield in the craton interior within the NE Gondwana continental block. However, lower
687
Paleozoic and lower-middle Mesozoic platform strata flanking this shield contributed the great
688
proportion of recycled sandy detritus according to the following argument. The proposed
689
Arabian Shield provenance terranes at the beginning of the Early Cretaceous was subjected to
690
uplift of the block faulted continental block due to continued breakup and rifting in NE
691
Gondwana, and an associated deep erosion. This tectonic uplift ceased gradually through the
692
Early Cretaceous Epoch, so that the relief of the Arabian Shield, as well as the Paleozoic and
693
older Mesozoic platform clastic strata became low, thus corresponding to the craton interior
694
provenance terrane of the continental block. Consequently, the retarded rate of erosion
695
contributed a wide spectrum of recycled sandy detritus including the monocrystalline and
696
polycrystalline quartz, K-feldspars, and plagioclase. They were subjected to an intense chemical
35
697
weathering due to the hot humid climate prevailing at the source rocks, during the long transit by
698
braided to low sinuosity streams that dispersed from the south-located Arabian Shield to the
699
north-located Neo-Tethys across continental surfaces of low slope. The humid hot or temperate
700
climate in the Early Cretaceous is indicated from the presence of carbonaceous shales and
701
lignites that are interbedded at several stratigraphic positions through the Kurnub Group (Amireh
702
and Abed, 1999). Moreover, the position of Jordan was located within the tropical zone during
703
the Early Cretaceous (Boucot et al., 2013).
704
This vigorous chemical weathering also acted at the depositional sites of the low-lying
705
braidplains, point bars, overbanks, and floodplains (Amireh, 1997, 2000; Amireh and Abed,
706
1999). Moreover, the recycled detritus was as well subjected to mechanical disintegration of the
707
labile feldspar grains along cleavage planes during the prolonged transport pathways. Under
708
these conditions of vigorous chemical weathering, and pronounced mechanical weathering,
709
acting on the recycled detritus, almost all the unstable feldspar grains and rock fragments were
710
destroyed, rendering the residual sediments only to the stable quartz varieties that gave rise
711
ultimately to the mature quartzarenites. However, some of the feldspar grains derived directly
712
from the granitoids and gneisses of the Arabian Shield (not recycled) might have escaped this
713
chemical and mechanical weathering and reached the marine intertidal-subtidal depositional
714
environment in Northern Jordan (profiles number 17-20, Fig. 2) to be deposited within the Jarash
715
and the Bir Fa‘as Formations (Appendix A.12).
716 717
Derivation of the detritus recycled from the Paleozoic and the older Mesozoic formations, or in other words, second-, or probably multi-cyclic origin of the major part of the sandstone
36
718
suite is indicated by the presence of two envelopes of syntaxial quartz overgrowths surrounding
719
the detrital quartz core (Fig. 7F). They represent two successive diagenetic stages that certainly
720
indicate two cycles of sedimentation. Moreover, the well roundness and the well sorting of the
721
quartz grains (Amireh, 2015) may substantiate the recycling origin of the sandstone. This is also
722
supported by detrital zircon U-Pb geochronology of the Lower Cretaceous sandstone of the
723
Kurnub Group west of study area (Kolodner et al., 2009). However, direct derivation of the
724
detritus from the Arabian Shield, and thus a first-cycle origin, cannot be excluded according to
725
the presence of few non-abraded, euhedral detrital zircon grains within the heavy mineral
726
fraction (Fig. 10E), and probably to the occurrence of some feldspar grains. The latter figure
727
shows that the majority of the heavy mineral grains consist of well-rounded, abraded zircon
728
grains that were probably recycled from the older sandstones.
729
730
8. Conclusions
731
1) The lower part of the uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan
732
constitutes a segment of the vast lower Paleozoic siliciclastic platform blanketing northern
733
Gondwana.
734
2) The Arabian Shield craton interior or the transitional group within the NE Gondwana
735
continental block represent the provenance terranes controlled by plate tectonics.
37
736
3) Braided rivers transported huge amounts of siliciclastic sediments and flew towards the north-
737
situated Paleo then Neo-Tethys during the early Paleozoic and the Early Cretaceous,
738
respectively.
739
4) Detrital framework modes of the siliciclastic sequence can be interpreted primarily in terms of
740
Dickinson‘s provenance terranes governed by plate tectonics.
741
5) The inferred recycled orogenic and magmatic arc provenances seem to be erroneous, due to
742
derivation of detritus from local syn-rift rhyolitic extrusions, not represented by plate tectonics-
743
provenance diagrams.
744
6) Immature rhyolitic litharenites and subarkosic arenites are interpreted in terms of basement
745
uplift continental block/local rhyolite extrusion, and transitional group provenances, respectively.
746
7) Super mature first-cycle, and second-cycle quartzarenites, were derived from stable carton
747
interior, and platform strata provenances, respectively, subjected to intense chemical weathering.
748
8) This work recommends to use Dickinson‘s petrographic model elsewhere with caution in
749
cases of intracratonic syn-rift volcanic provenances not represented in the plate tectonics-
750
provenance diagrams, and in cases of extraordinary effect of glacial paleoclimate.
751
752
753
38
754
Acknowledgments
755
The Deanship of Academic Research of the University of Jordan funds the research. Miss. Saja
756
Abu Taha is acknowledged for her assistance in the field and laboratory works, drawing the
757
graphs, and preparing the figures. Thanks for two anonymous reviewers for their valuable
758
comments that improved the paper, and for the editorial team of the Journal of Asian Earth
759
Sciences for their patience during the various phases of manuscript‘s review.
760
761
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762
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1063
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1064
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1071
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1096
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1100
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1105
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1107
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1109
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1110
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1111
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1113
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1114
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1115
59
1116
Zuffa, G.G., 1985. Optical analyses of arenites: influence of methodology on compositional
1117
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1118
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1119
1120
Figure captions
1121
Fig. 1. A simplified geological map of North Africa and Arabia illustrating the distribution of
1122
Precambrian (cratonic basement, remobilized during Pan African orogeny, Pan African juvenile
1123
crust) outcrops including the Arabian Shield, Nubian Shield, Leo Shield, Saharan Metacraton,
1124
West African Craton, Tanzania-Congo Craton, Paleozoic, Mesozoic sedimentary rocks and
1125
Cenozoic sediments and basalt and sedimentary rocks, and location of study area in Jordan
1126
(modified from Alsharhan and Nairn, 1997 (Paleozoic, Mesozoic and Cenozoic outcrops in
1127
Arabia), Avigad et al., 2003 (Precambrian outcrops in Africa), Johnson et al., 2011 (Precambrian
1128
outcrops in Arabia and Nubia), and Viljoen, 2016 (Paleozoic, Mesozoic and Cenozoic outcrops
1129
in Africa). S= Sarmuj; E= Elat; NG= Negev; J= Jibalah; TH= Talbah Group; WH= Wadi Halfa;
1130
T.= terrane.
1131
Fig. 2. Geological map of Jordan demonstrating the outcrops of the Neoproterozoic basement
1132
complex (Aqaba and Araba Complexes), and Neoproterozoic Aheimir Volcanic Suite; outcrops
1133
of the Cambrian, Ordovician, and Silurian Systems, Lower Cretaceous Series (modified from
1134
Amireh, 2000, Amireh et al., 2001); paleocurrent directions during late Ediacaran-early
1135
Cambrian (pink colored arrow), Cambrian (purple colored arrows), Ordovician (red colored
60
1136
arrows), Early Cretaceous (black colored arrows); position of HM-2, AJ-1, NH-1, and WS-3 oil
1137
discovering wells, and position of investigated profiles: 1= Salab Fm.; 2= Umm Ishrin Fm.; 3=
1138
Disi Fm.; 4= Umm Saham Fm.; 5= Hiswa Fm.; 6= Dubaydib Fm.; 7= Tubailiyat Mb. of
1139
Mudawwara Fm. and KG; 8= Ammar Mb.; 9= Batra Mb. and KG, 10= Ratya Mb.; 11= Khusha
1140
Fm.; 12= Abu Khusheiba Fm. and Umm Ghaddah Fm.; 13= Umm Ghaddah Fm. in Wadi Umm
1141
Ghaddah; 14= Salab Fm., Burj Fm., Abu Khusheiba Fm., Umm Ishrin Fm., and KG in Dana
1142
area; 15= KG in Wadi Karak; 16= Umm Ghaddah Fm. in Wadi Al Mahrakah: 17= KG in Na‘ur;
1143
18= KG in Jarash; 19= KG in A‘arda; 20= KG in O‘ion Musa; S= Sarmuj Conglomerate Fm;
1144
Fm.= Formation; Mb.= Member; KG= Kurnub Group.
1145
Fig. 3. Stratigraphic subdivisions of the uppermost Ediacaran-Lower Cretaceous clastic sequence
1146
of Jordan, and the five sandstone suites (sandstone suite #1- sandstone suite #5) assigned in the
1147
present study.
1148
Fig. 4. Outcrop photographs for some of the formations of the uppermost Ediacaran-Lower
1149
Cretaceous clastic sequence.
1150
(A) Irregular contact (paleorelief) between the upper Ediacaran Aheimir Volcanic suite and the
1151
uppermost Ediacaran-lower Cambrian Umm Ghaddah Formation; person as scale is ca 1.8 m.
1152
(B) Nonconformity (Rum unconformity, Powell et al., 2014) in form of a peneplain (arrow)
1153
between the Neoproterozoic Aqaba Complex and the Fortunian Salab Formation; width of
1154
outcrop is ca 500 m.
61
1155
(C) Contacts between the Neoproterozoic Aqaba Complex, Salab, Burj, Abu Khusheiba, and
1156
Umm Ishrin Formations in Dana Area (profile number 14); height of the tree at lower central part
1157
of the photo attains ca 1.5 m.
1158
(D) Deformed cross-bedding characterizing Umm Ishrin Formation, pencil is ca 15 cm.
1159
(E) A storm channel interbedded within intertidal flat facies of Dubaydib Formation, width of
1160
outcrop is ca 15 m.
1161
(F) A volcanic tuff and a volcaniclastic conglomerate interbedded within the cross-bedded
1162
(CBSS) and horizontal bedded (HBSS) sandstone of the Burj Formation; length of geologic
1163
hammer is 30 cm.
1164
Fig. 5. Tectono sedimentary block diagrams illustrating development of the tectonic-controlled
1165
provenance and the depositional environments through time slices of the late Ediacaran-Late
1166
Cretaceous, corresponding to the five sandstone suites; C.B.= continental block.
1167
(A) Late Ediacaran-early Cambrian time of Umm Ghaddah Formation (SS suite #1). Violet
1168
arrows indicate direction of regional crustal extension (modified from Amireh et al., 2008).
1169
(B) Early-mid Cambrian time of Salab, Abu Khusheiba and Burj Formations (SS suite #2)
1170
(modified from Amireh et al., 1994b).
1171
(C) Late Cambrian-Mid Ordovician time of Umm Ishrin, Disi and Umm Saham Formations (SS
1172
suite #3). CH= channel architectural element, LS= laminated sand sheet, DA= downstream
1173
accretion macroform, FF= over bank fine sediments (modified from Amireh et al., 2001).
62
1174
(D) Mid Ordovician-mid Silurian time of Hiswa, Dubaydib, Mudawwara, and Khusha
1175
Formations (SS suite #4). SF= sandy tidal flat, MF= mixed tidal flat (modified from Amireh et
1176
al., 2001).
1177
(E) Early Cretaceous time of Jarash Formation of the Kurnub Group (SS suite #5) (modified
1178
from Amireh and Abed, 1999).
1179
Fig. 6. Modified sandstone classification of Pettijohn et al. (1987) depicting the types of
1180
sandstone for the means of the members, formations, and groups of the clastic sequence under
1181
investigation; Q= total quartz, F= total feldspars, R= lithic fragments (L).
1182
Fig. 7. Thin section photomicrographs illustrating:
1183
(A) Quartzarenite of Umm Ishrin Formation showing detrital matrix (M) filling passively
1184
interstitial spaces between detrital monocrystalline quartz grains (Qm) without altering the quartz
1185
detrital cores (Qdc)or even the quartz overgrowths (Qog), plane polarized light.
1186
(B) Quartzarenite of Ramel Formation of the Kurnub Group illustrating quartz overgrowth
1187
cement (Qov) filling completely interstitial spaces between detrital monocrystalline quartz grains
1188
without altering them, crossed polarized light.
1189
(C) Quartzarenite of Umm Saham Formation showing iron oxide cement (FeC) filling passively
1190
interstitial spaces between detrital quartz grains (Qm) without altering the quartz grains, pore
1191
space (PS) is left without being filled with cement, plane polarized light.
63
1192
(D) Subarkosic arenite of Dubaydib Formation showing dolomite cement (DC) that corrodes the
1193
framework grains of quartz (Qcorr) and feldspar grains (F) but keeping them unaltered to be
1194
correctly identified, air bubble (AB), crossed polarized light.
1195
(E) Quartzarenite of Karak Formation of the Kurnub Group consisting entirely of quartz
1196
framework grains, particularly monocrystalline quartz cemented by calcite (CC); note corrosion
1197
of a quartz grain (Qcorr) leaving just two patches that are still identifiable (at complete extinction
1198
position), crossed polarized light.
1199
(F) Second-cycle quartzarenite of Karak Formation of the Kurnub Group consisting of
1200
monocrystalline quartz grains characterized by two stages of syntaxial quartz overgrowths. The
1201
first stage overgrowth is separated from the detrital core (Qdc) by the dust line number 1 (DL
1202
#1), and the second stage overgrowth is separated from the first stage by the dust line number 2
1203
(DL #2), crossed polarized light.
1204
Fig. 8. Thin section photomicrographs illustrating:
1205
(A) A polycrystalline quartz (Qp) consisting of equigranular quartz crystals of probably a
1206
metamorphic sandstone origin, and a monocrystalline quartz (Qm) in quartzarenite of Umm
1207
Ishrin Formation, crossed polarized light.
1208
(B) A polycrystalline quartz grain (Qp) consisting of quartz crystals with sutured contacts and a
1209
preferred orientation indicating a foliated metamorphic origin in rhyolitic litharenite of Umm
1210
Ghaddah Formation, crossed polarized light.
64
1211
(C) Chert lithic fragment (Ch) characterized by the clear appearance of quartz and the
1212
microcrystalline texture, and a devitrified rhyolitic lithic fragment (DRL) distinguished by the
1213
brownish turbid appearance and the felsitic texture consisting of cryptocrystalline quartz crystals
1214
smaller than that of chert, in rhyolitic litharenite of Umm Ghaddah Formation, plane polarized
1215
light.
1216
(D) Same as Fig. 8C but under crossed polarized light. Note the obvious contrast between the
1217
quartz microcrystals in extinction and illumination positions characterizing the chert lithic
1218
fragment.
1219
(E) Orthoclase grains (Or) with multiple twinning (mt) and simple twinning (st), and
1220
monocrystalline quartz (Qm) in subarkosic arenite of the Salab Formation, crossed polarized
1221
light.
1222
(F) A microcline grain (Mc) characterized by cross-hatching twinning and monocrystalline
1223
quartz (Qm) and another feldspar grain (F) in a subarkosic arenite of the Salab Formation with,
1224
crossed polarized light.
1225
Fig. 9. Thin section photomicrographs showing:
1226
(A) A devitrified rhyolitic lithic fragment (DRL) with glass shards (GS) that are also devitrified,
1227
and a chert fragment (Ch) in rhyolitic litharenite of Umm Ghaddah Formation, plane polarized
1228
light.
65
1229
(B) Same as Fig. 9A but under crossed polarized light. Note the devitrification of both the
1230
rhyolitic clast (DRL) and the included glass shards (GS) giving rise to microgranular felsitic
1231
texture consisting of cryptocrystalline quartz crystals that are smaller than that of the chert
1232
fragment.
1233
(C) A devitrified rhyolitic lithic fragment (DRL) consisting of phenocrysts (probably an euhedral
1234
feldspar phenocryst, FPhC) and irregular shaped pyroclastic phenocryst (PPhC) that are bound
1235
by a devitrified ground mass (DGM), which is set in a detrital matrix (DtM) in rhyolitic
1236
litharenite of Umm Ghaddah Formation, plane polarized light.
1237
(D) Same as Fig. 9C but under crossed polarized light. Note the devitrification of the phenocrysts
1238
and ground mass within the rhyolitic lithic fragment, and the silt-sized detrital quartz grains in
1239
the detrital matrix.
1240
(E) A rhyolitic lithic fragment exhibiting a spherulitic texture (SphRL) and a devitrified volcanic
1241
lithic fragment (DVL) characterized by microfelsitic texture in rhyolitic litharenite of Umm
1242
Ghaddah Formation, crossed polarized light.
1243
(F) A mafic clast composed of devitrified feldspar laths (DFL) and anhedral phenocryst (APhC)
1244
set in opaque groundmass in rhyolitic litharenite of Umm Ghaddah Formation, plane polarized
1245
light.
1246
Fig. 10. Thin section photomicrographs illustrating:
66
1247
(A) A silty mudstone lithic fragment constituted mainly of silt-sized grains (SSG) and a few fine
1248
sand grains (FSG) bound by a clayey matrix (ClM) in the rhyolitic litharenite of Umm Ghaddah
1249
Formation, plane polarized light.
1250
(B) Same as Fig. 10A but under crossed polarized light. Note the first order interference color of
1251
the silt and sand sized grains, and the cryptocrystalline nature of the clayey matrix.
1252
(C) A schist grain consisting of foliated aggregates of quartz and mica crystals in the rhyolitic
1253
litharenite of Umm Ghaddah Formation, plane polarized light.
1254
(D) Same as Fig. 10C but under crossed polarized light.
1255
(E) Euhedral detrital zircon grain (EZ) derived directly from the Arabian Shield and several
1256
rounded zircon grains (RZ) recycled from Paleozoic and Mesozoic strata, and a rutile grain (R)
1257
in the Karak Formation of the Kurnub Group, grain mount, plane polarized light.
1258
(F) An apatite grain characterized by two stages of apatite overgrowths; apatite overgrowth
1259
number 1 (Aog #1) and apatite overgrowth number 2 (Aog #2) enveloping an apatite detrital core
1260
(Adc) in the subarkosic arenite of Salab Formation, plane polarized light.
1261
Fig. 11. Triangular compositional plots showing mean framework modes for all the members,
1262
formations, and groups of the upper Ediacaran-Lower Cretaceous clastic sequence. (A) QtFL,
1263
(B) QmFLt, (C) QpLvLs, and (D) QmPK. Division lines are after Dickinson and Suczek (1979)
1264
and Dickinson et al., (1983), and in percentage units measured from nearest apical pole. For
1265
number of samples in each member, formation or group see Table 2.
67
1266
1267
Table captions
1268
Table 1. Paleocurrent directions based on 1339 measurements of azimuths of planar and trough
1269
cross bedding (complied from Amireh 1993, 1997, 2000; Amireh et al., 1994a, 2001, 2008;
1270
Amireh and Abed, 1998)
1271
Table 2. Mean, standard deviation (STDEV. S), confidence level (95%) of framework modes for the
1272
members/formations/groups of the uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of
1273
Jordan
1274
1275
Vitae
1276
Belal S. Amireh graduated from the University of Jordan in geology and mineralogy in 1977,
1277
and obtained M.Sc. from the same university in sedimentology and petrography of oil shale in
1278
1979. Amireh received his Ph.D. from the Technical University of Braunschweig in Germany in
1279
sedimentology and petrology of clastic deposits in 1987. He was appointed as an Assistant Prof.
1280
in the University of Jordan in 1991, promoted to an Associate Prof. in 1996, and to a Professor in
1281
2001, where he is still now at this position. Amireh published many articles in international
1282
journals in the field of sedimentology, mineralogy, and geochemistry of clastic deposits.
1283
68
1284 1285
69
1286 1287
70
1288 1289
71
1290 1291
72
1292 1293
73
1294 1295
74
1296 1297
75
1298 1299
76
1300 1301
77
1302 1303
78
1304
79
Table 1. Paleocurrent directions based on 1339 measurements of azimuths of planar and trough cross bedding (complied from Amireh 1993, 1997, 2000; Amireh et al., 1994b, 2001, 2008; Amireh and Abed, 1999)
Age
Form-
Locality
ation
Readings Mean
number
Direction
Age
Form- Locality
Readings Mean
ation
number
direction
LEd-eCamb
UG
W. el Mahrakah
48
55 NE
ECretaceous KG
Mollightah
24
N
Cambrian
S + UI
Rum-Ras Naqab
153
N
ECretaceous KG
W. Dana
33
13 NW
Cambrian
AKh
W. A Khusheiba
96
5 NE
ECretaceous KG
W. Khuneizirah 35
10 NW
Cambrian
S+AKh Dana
113
12 NW
ECretaceous KG
Afra
42
5 NW
Cambrian
S+AKh Safi
12
10 NW
ECretaceous KG
W. el Hasa
28
N
Cambrian
UI
W. Zarq-Ma‘in
44
30 NW
ECretaceous KG
W. Nummeirah
39
5 NW
Ordovician
Disi
Disi-W. Hasa
50
5 NW
ECretaceous KG
W. Isal
38
N
Ordovician
US
G.Gh.-Ras Naqab
77
N
ECretaceous KG
W. el Karak
30
9 NW
Ordovician
Disi
Disi-W.Nummeira 42
6 NW
ECretaceous KG
Hamm. Ma‘in
31
10 NW
W.Mash-W.Karak
12 NW
ECretaceous KG
O‘ion Musa
19
7 NW
ECretaceous KG
80
80
ECretaceous KG
W. Mashabah
6
8 NW
ECretaceous KG
Nau‘r
41
N
ECretaceous KG
Rasen Naqab
14
N
ECretaceous KG
Mahis
20
13 NW
ECretaceous KG
W. Rakeya
3
N
ECretaceous KG
Baqa‘a
42
N
ECretaceous KG
W. Qsieb
23
6 NW
ECretaceous KG
Jarash
53
20 NW
ECretaceous KG
Dillaghah
6
10 NW
ECretaceous KG
A‘arda
77
22 NW
ECretaceous KG
Petra
20
8 NW
Total number of measurements= 1339; LEd-eCamb= late Ediacaran-early Cambrian; ECretaceous= Early Cretaceous; UG= Umm Ghaddah Fm., S= Salab Fm., UI= Umm Ishrin Fm., AKh= Abu Khusheiba Fm., US= Umm Saham Fm., KG= Kurnub Group; for localities of formations or KG see Fig. 2 and Amireh (1993, 2000).
81
Table 2. Mean, standard deviation (STDEV. S), confidence level (95%) of framework modes for the members/formations/groups of the uppermost Ediacaran-Lower Cretaceous siliciclastic sequence of Jordan Mb./Fm./G. UG Fm. M (n= 60) STDEV.S C. l. 95% Salab Fm. M (n= 68) STDEV.S C. l. 95% Burj Fm. M (n= 11) STDEV.S C. l. 95% AK Fm. M (n= 20) STD.P C.L.95% UI Fm. M (n= 35) STDEV.S C. l. 95% Disi Fm. M (n= 16) STDEV.S
FW
Mt C
Qt
F
L
Qm
F
Lt
Qp
Lv
Ls
Qm
P
K
81.0 8.8 10.2 43.0 12.6 44.4 38.5 12.6 48.9 10.1 4.9 3.8 4.5 13.0 8.4 16.2 12.1 8.4 15.5 6.6 1.3 1.0 1.2 3.4 2.2 4.2 3.1 2.2 4.0 1.7
82.5 7.4 77.3 8.9 5.7 13.7 2.3 1.5 3.5
2.7 20.0 2.6 11.9 0.7 3.1
80.2 7.9 11.9 77.8 17.2 5.0 5.3 4.3 6.1 10.2 7.4 6.3 1.3 1.0 1.5 2.5 1.8 1.5
29.6 0.4 79.8 28.3 1.9 8.8 7 0.5 2.1
1.4 18.8 1.5 8.2 0.4 2.0
61.9 4.1 88.7 31.6 4.4 4.5 21.2 3.0 3.0
0.5 10.8 0.8 4.7 0.5 3.2
12.9 0.6 88.1 17.2 1.6 5.6 8.3 0.8 2.6
0.6 11.3 0.9 5.2 0.4 2.4
74.1 0.8 25.1 70.5 7.5 7.6 1.5 7.8 20.6 3.8 5.1 1.0 5.2 13.8 2.6
69.2 17.2 13.6 70.0 11 7.4 8.4 28.7 2.7 1.8 2.0 7.1
22.0 65.0 7.5 22.4 19.3 3.8 15.0 13.0 2.6
27.5 34.0 20.9 34.4 14.0 23.1
80.3 5.1 14.6 87.2 11.0 1.8 4.5 5.1 4.2 5.8 4.8 3.6 2.1 2.4 1.9 2.7 2.3 1.7
81.6 11.0 7.4 8.9 4.8 6.4 4.2 2.3 3.0
86.5 18.3 8.8
77.2 3.0 19.8 99.7 0.0 3.5 3.0 4.6 0.8 0.0 1.2 1.0 1.6 0.3
0.3 0.8 0.3
87.1 0.0 8.6 0.0 3.0
12.9 98.1 8.6 4.0 3.0 1.4
1.9 4.0 1.4
0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0
77.3 1.7 21.0 99.7 0.0 5.4 2.5 5.2 0.4 0.0
0.3 0.4
86.1 0.0 9.1 0.0
13.9 98.5 9.1 3.1
1.5 3.1
0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0
82
C. l. 95% US Fm. M (n= 25) STDEV.S C. l. 95% Hiswa Fm. M (n= 9) STDEV.S C. l. 95% Dub. Fm. M (n= 31) STDEV.S C. l. 95% Mudw. Fm. M (n= 31) STDEV.S Conf.l.95 Khu. Fm. M (n= 7) STDEV.S C. l. 95% Kurnub G. M (n= 28) STDEV.S C. l. 95%
2.9
1.3 2.8
0.2
83.0 0.6 16.4 99.9 0.0 4.7 1.3 3.7 0.4 0.0 1.9 0.5 1.5 0.2
0.2
4.8
4.8
1.5
1.5
0.1 0.4 0.2
92.3 0.0 4.2 0.0 1.7
7.7 4.2 1.7
99.5 2.4 1.0
0.5 2.4 1.0
0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0
76.0 5.8 18.2 86.2 13.6 0.2 4.4 8.6 8.7 6.0 6.3 0.7 3.4 6.6 6.7 4.6 4.8 0.5
84.4 13.6 2.0 6.4 6.3 2.4 4.9 4.8 1.8
100.0 0.0 0.0 0.0
0.0 85.8 0.0 7.0 5.4
0.6 13.6 1.0 6.3 0.8 4.8
83.7 1.6 14.7 79.4 20.6 0.0 6.7 2.5 7.0 8.4 8.4 0.0 2.5 0.9 2.6 3.1 3.1
76.5 20.6 2.9 8.8 8.4 2.2 3.2 3.1 0.8
100.0 0.0 0.0 0.0
0.0 78.8 0.0 8.8 3.2
0.5 20.7 0.6 8.5 0.2 3.1
81.8 2.3 15.9 78.0 22.0 0.0 7.0 4.1 6.4 5.9 5.9 0.0 2.6 1.5 2.3 2.2 2.2
75.0 22.0 3.0 4.9 5.9 2.5 1.8 2.2 0.9
100.0 0.0 0.0 0.0
0.0 77.3 0.0 5.9 2.2
0.2 22.5 0.4 5.9 0.1 2.2
87.0 0.6 12.4 81.3 18.7 0.0 3.8 1.5 2.7 2.9 2.9 0.0 3.5 1.4 2.5 2.7 2.7
79.9 18.7 1.4 4.6 2.9 1.8 4.3 2.7 1.7
100.0 0.0 0.0 0.0
0.0 80.8 0.0 3.2 3.0
0.3 18.9 0.5 3.0 0.5 2.8
84.4 4.3 11.3 99.7 0.3 7.0 5.6 7.0 0.9 0.9 2.7 2.2 2.7 0.3 0.3
96.2 0.3 2.4 0.9 0.9 0.3
100.0 0.0 0.0 0.0
0.0 99.7 0.0 0.0
0.0 0.3 0.0 0.0
0.0 0.0
3.5 2.4 0.9
Mb.= Member; Fm.= Formation; G.= Group; FW= framework grains; Mt= detrital matrix ; C= total cements; Qt= total quartz; F= total feldspar; L= lithic fragments; Qm= monocrystalline quartz; Qp= polycrystalline quartz; Lt= total lithic grains; Lv= volcanic lithic fragments; Ls= sedimentary lithic fragments; P= plagioclase; K= K-feldspar; M= mean; n= number of samples; UG= Umm Ghaddah; AK= Abu Khusheiba; UI= Umm Ishrin; US= Umm Saham; Dub.= Dubaydib; Mudw.= Mudawwara; and Khu.= Khusha.
83
Appendix A. Mean, standard deviation (STDEV. S), confidence level (95%) of the framework modes for all samples in each of the groups/formations/members of the uppermost EdiacaranLower Cretaceous clastic sequence A.1 Umm Ghaddah Formation S.N. UG3 UG4 UG5 UG6 UG7 UG8 F. B AJ3791 AJ3791 AJ3790 AJ3750 AJ3706 AJ3694 AJ3650 AJ3590 AJ3560 AJ3500 AJ3470 AJ3410 AJ3350 AJ3280 AJ3240 AJ3200 AJ3160 AJ3130 AJ3100 AJ3070 AJ3055 AJ3035 AJ3015 AJ2995 AJ2982 AJ2980 AJ2978 AJ2975 NH3960 NH3850 NH3700 NH3659 NH3656
FW 86 89 87 88 91 87 77 75 75 79 75 84 80 82 79 74 80 79 75 83 87 82 83 79 88 85 84 86 85 84 91 86 87 89 87 80 79 80 86 78
Mt 6 7 5 5 4 4 8 17 5 13 10 0 16 8 7 9 10 10 12 6 4 6 5 4 7 4 7 5 9 6 7 9 10 7 8 12 9 11 8 15
C 8 4 8 7 5 9 15 8 20 8 15 16 4 10 14 17 10 11 13 11 9 12 12 17 5 11 9 9 6 10 2 5 3 4 5 8 12 9 6 7
Qt 13 40 47 2 48 26 60 27 21 18 39 33 44 41 35 45 45 57 49 70 30 62 54 67 53 59 58 54 48 64 65 43 41 44 43 33 27 34 45 46
F 6 1 0 0 1 2 14 0 0 0 9 0 10 9 5 17 14 5 12 6 3 10 12 10 15 7 7 6 12 7 8 6 11 7 14 20 19 18 20 22
L 81 59 53 98 51 72 26 73 79 82 52 67 46 50 60 38 41 38 39 24 67 28 34 23 32 34 35 40 40 29 27 51 48 49 43 47 54 48 35 32
Qm 12 39 45 2 47 26 57 25 17 14 34 25 36 38 29 33 40 53 45 60 28 61 48 58 50 54 49 47 42 57 62 34 37 35 39 30 24 31 37 42
F 6 1 0 0 1 2 14 0 0 0 9 0 10 9 5 17 14 5 12 6 3 10 12 10 15 7 7 6 12 7 8 6 11 7 14 20 19 18 20 22
Lt 82 60 55 98 52 72 29 75 83 86 57 75 54 53 66 50 46 42 43 34 69 29 40 32 35 39 44 47 46 36 30 60 52 58 47 50 57 51 43 36
Qp 1 2 2 0 2 0 9 4 5 5 7 11 14 7 9 23 11 9 9 28 3 4 15 28 9 12 22 15 13 19 7 15 9 15 10 7 5 5 19 11
Lv 93 94 90 97 96 94 86 87 85 88 80 83 77 86 81 68 84 85 88 68 87 83 73 64 81 76 73 72 77 68 74 64 62 71 83 93 93 95 78 86
Ls 6 4 8 3 2 6 5 9 10 7 13 6 9 7 10 9 5 6 3 4 10 13 12 8 10 12 5 13 10 13 19 21 29 14 7 0 2 0 3 3
Qm 67 97 100 100 98 92 80 100 100 100 80 100 78 82 85 66 74 91 78 91 89 86 80 85 77 88 87 89 78 89 89 85 76 84 74 60 56 64 65 66
P 0 0 0 0 0 0 0 0 0 0 3 0 6 5 0 6 5 0 5 0 0 2 2 0 5 0 2 0 4 0 3 0 2 3 4 8 9 3 4 6
K 33 3 0 0 2 8 20 0 0 0 17 0 16 13 15 28 21 9 17 9 11 12 18 15 18 12 11 11 18 11 8 15 22 13 22 32 35 33 31 28
84
NH3653 NH3651 NH3500 NH3391 NH3389 NH3385 HM1450 HM1400 HM1329 HM1275 HM1270 HM1268 HM1197 HM1196 HM1192 WS4527 WS4500 WS4374 WS4300 WS4217 M (n= 60) STDEV.S C. l. 95%
79 76 78 75 78 79 82 81 76 75 80 73 76 81 75 75 77 81 75 75 81.0 4.9 1.3
14 15 14 10 10 13 10 12 17 3 5 7 9 7 7 13 9 11 14 13 8.8 3.8 1.0
7 9 8 15 12 8 8 7 7 22 15 20 15 12 18 12 14 8 11 12 10.2 4.5 1.2
39 45 33 59 42 52 41 42 36 41 33 35 45 35 40 48 48 40 52 43 43.0 13.0 3.4
22 12 26 20 23 25 10 11 21 22 23 20 18 30 24 28 22 25 9 21 12.6 8.4 2.2
39 43 41 21 35 23 49 47 43 37 44 45 37 35 36 24 30 35 39 36 44.4 16.2 4.2
34 42 29 53 37 46 37 33 30 37 31 32 44 35 38 44 44 37 47 39 38.5 12.1 3.1
22 12 26 20 23 25 10 11 21 22 23 20 18 30 24 28 22 25 9 21 12.6 8.4 2.2
44 46 45 27 40 29 53 56 49 41 46 48 38 35 38 28 34 38 44 40 48.9 15.5 4.0
14 6 8 21 13 22 9 16 11 10 3 6 2 0 7 14 11 10 12 10 10.1 6.6 1.7
86 94 89 79 87 78 82 73 81 73 86 82 93 96 93 76 85 90 82 83 82.5 8.9 2.3
0 0 3 0 0 0 9 11 8 17 11 12 5 4 0 10 4 0 6 7 7.4 5.7 1.5
62 78 53 73 62 64 79 75 59 63 58 62 70 55 62 60 67 60 83 66 77.3 13.7 3.5
2 0 7 2 4 5 3 0 5 2 7 5 2 7 2 6 4 6 0 5 2.7 2.6 0.7
36 22 40 25 34 31 18 25 36 35 35 33 28 38 36 34 29 34 17 29 20.0 11.9 3.1
Qt 68 78 85 88 71 80 82 82 78 94 81 86 87 61 67 69 85 70
F 29 19 15 12 26 19 15 18 18 6 7 5 13 29 32 16 12 23
L 3 3 0 0 3 1 3 0 4 0 12 9 0 10 1 15 3 7
Qm 55 59 70 68 60 78 80 79 75 94 81 86 84 53 57 59 72 65
F 29 19 15 12 26 19 15 18 18 6 7 5 13 29 32 16 12 23
Lt 16 22 15 20 14 3 5 3 7 0 12 9 3 18 11 25 16 12
Qp 79 84 100 100 82 50 50 100 50 0 0 0 100 46 87 41 83 44
Lv 21 16 0 0 18 50 50 0 50 0 100 100 0 54 13 59 17 56
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 66 76 83 85 70 80 84 81 80 94 92 94 87 65 64 78 85 73
P 0 0 0 0 0 3 3 0 3 0 0 0 0 3 5 2 0 5
K 34 24 17 15 30 17 13 19 17 6 8 6 13 32 31 20 15 22
A.2 Salab Formation S.N. SD1 SD2 SD3 SD4 SD5 SD6 SD7 SD8 SD9 SD10 SD11 SD12 SD13 LCD1 LCD2 LCD6 LCD11 LCD14
FW 87 86 81 81 78 77 79 76 83 81 85 91 86 74 75 72 75 74
Mt 6 5 9 9 8 7 9 7 6 8 5 0 5 10 10 10 0 7
C 7 9 10 10 14 16 12 17 11 11 10 9 9 16 15 18 25 19
85
LCD16 LCD20 LCD29 LCD32 SR1 SR2 SR3 SR4 SR5 SR6 SR11 LCR3 LCR5 LCR6 LCR7 LCR9 LCR14 LCR18 AJ2930 AJ2880 AJ2820 AJ2780 AJ2760 AJ2710 AJ2680 AJ2640 AJ2600 NH3100 NH3000 NH2867 NH2866 NH2864 NH2860 NH2400 HM953 HM882 HM798 HM680 HM582 HM428 HM420 HM410 WS4200 WS4150 WS4050 WS3950 WS3850 WS3800
79 76 73 78 73 77 78 75 76 80 75 83 76 75 76 78 80 76 87 91 86 88 85 87 90 84 83 78 75 77 81 77 74 77 84 91 92 88 91 82 79 80 81 76 81 77 78 75
0 0 16 3 9 8 10 10 9 6 10 1 2 2 3 3 0 0 10 8 12 11 13 7 4 12 11 12 13 11 8 8 17 15 11 5 4 8 5 8 8 10 10 14 12 15 12 12
21 24 11 19 18 15 12 15 15 14 15 16 22 23 21 19 20 24 3 1 2 1 2 6 6 4 6 10 12 12 11 15 9 8 5 4 4 4 4 10 13 10 9 10 7 8 10 13
67 86 79 85 89 77 64 80 79 94 50 86 81 70 73 81 82 92 72 81 81 84 86 79 89 92 71 46 63 61 64 60 74 81 73 85 87 87 93 82 78 92 73 68 79 72 85 68
6 14 21 15 8 18 29 20 21 6 26 14 19 30 27 19 18 8 13 9 19 13 9 21 7 6 24 32 24 23 20 26 18 19 19 10 8 6 5 17 18 8 20 24 12 22 15 29
27 0 0 0 3 5 7 0 0 0 24 0 0 0 0 0 0 0 15 10 0 3 5 0 4 2 5 22 13 16 16 14 8 0 8 5 5 7 2 1 4 0 7 8 9 6 0 3
48 59 65 81 85 72 54 76 79 94 44 74 76 63 71 72 77 79 70 73 78 78 76 68 75 75 65 44 52 58 55 52 65 71 66 58 77 76 80 72 59 79 64 62 72 61 70 60
6 14 21 15 8 18 29 20 21 6 26 14 19 30 27 19 18 8 13 9 19 13 9 21 7 6 24 32 24 23 20 26 18 19 19 10 8 6 5 17 18 8 20 24 12 22 15 29
46 27 14 4 7 10 17 4 0 0 30 12 5 7 3 9 5 13 17 18 3 9 15 11 18 19 11 24 24 19 25 22 17 10 15 32 15 18 15 11 23 13 16 14 16 17 15 11
42 100 100 100 60 50 59 100 0 0 45 100 100 100 100 100 100 100 13 44 100 62 69 100 75 87 56 11 47 20 37 35 50 100 46 83 64 62 86 89 83 100 54 45 46 62 100 75
58 0 0 0 40 50 41 0 0 0 49 0 0 0 0 0 0 0 87 56 0 38 31 0 25 13 44 89 53 73 63 53 50 0 54 17 36 38 14 11 17 0 46 55 54 38 0 25
0 0 0 0 0 0 0 0 0 0 6 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 7 0 12 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
88 81 75 84 91 80 65 79 79 94 63 83 80 68 73 79 82 90 85 89 81 86 89 76 92 93 73 58 69 71 73 67 78 78 77 85 91 93 95 81 77 91 76 80 75 73 82 67
0 0 5 1 0 0 0 0 1 0 0 3 0 3 1 1 1 2 1 0 2 1 0 3 0 0 3 3 2 3 2 3 3 2 0 2 0 0 0 3 2 0 2 1 3 1 0 3
12 19 20 15 9 20 35 21 20 6 37 14 20 29 26 20 17 8 14 11 17 13 11 21 8 7 24 39 29 26 25 30 19 20 23 13 9 7 5 16 21 9 22 19 22 25 18 30
86
WS3718 WS3713 M (n= 68) STDEV.S C. l. 95%
79 77 80.2 5.3 1.3
3 14 7.9 4.3 1.0
18 9 11.9 6.1 1.5
81 77 77.8 10.2 2.5
19 23 17.2 7.4 1.8
0 0 5.0 6.3 1.5
77 71 69.2 11 2.7
19 23 17.2 7.4 1.8
4 6 13.6 8.4 2.0
C 14 18 28 30 22 18 30 42 27 20 27 25.1 7.8 5.2
Qt 89 84 85 81 90 85 56 76 40 32 58 70.5 20.6 13.8
F 9 16 11 4 5 9 4 5 5 5 9 7.5 3.8 2.6
L 2 0 4 15 5 6 40 19 55 63 33 22.0 22.4 15.0
Qm 75 72 80 74 86 84 54 72 35 29 55 65.0 19.3 13.0
F 9 16 11 4 5 9 4 5 5 5 9 7.5 3.8 2.6
Lt 16 12 9 22 9 7 42 23 60 66 36 27.5 20.9 14.0
F 13 6 15 11 13 10 7 7 5 9 7 10 14 16 6 4
L 0 0 0 0 0 0 0 0 0 0 2 15 7 4 4 3
Qm 84 94 81 88 84 79 93 92 94 90 85 64 73 75 83 85
F 13 6 15 11 13 10 7 7 5 9 7 10 14 16 6 4
Lt 3 0 4 1 3 11 0 1 1 1 8 26 13 9 11 11
100 100 70.0 28.7 7.1
0 0 29.6 28.3 7
0 0 0.4 1.9 0.5
80 75 79.8 8.8 2.1
1 3 1.4 1.5 0.4
19 22 18.8 8.2 2.0
A.3 Burj Formation S.N. MCD29 MCD32 MCD38 MCD34 MCD42 MCD43 MCD44 MCD50 B1 B3 B4 M (n= 11) STDEV.S C. l. 95%
FW 81 81 70 70 77 82 70 56 73 80 73 74.1 7.6 5.1
Mt 5 1 2 0 1 0 0 0 0 0 0 0.8 1.5 1.0
Qp 92 100 50 32 43 17 4 15 9 4 8 34.0 34.4 23.1
Lv 8 0 50 60 57 83 86 77 89 86 85 61.9 31.6 21.2
Ls 0 0 0 8 0 0 10 8 2 10 7 4.1 4.4 3.0
Qm 89 82 87 94 94 91 92 93 86 82 85 88.7 4.5 3.0
P 2 0 2 1 0 0 0 0 0 0 0 0.5 0.8 0.5
K 9 18 11 5 6 9 7 7 14 18 15 10.8 4.7 3.2
A.4 Abu Khusheiba Formation S.N. AK1 AK2 AK3 AK4 AK5 Ak6 AK7 AK8 AK9 AK10 MCKS2 MCKS6 MCKS10 MCKS13 MCKS16 MCKS18
FW 78 83 82 85 75 74 75 75 83 82 86 89 76 83 84 80
Mt 8 5 5 5 7 8 9 9 0 0 2 0 8 0 1 10
C 14 12 13 10 18 18 16 16 17 18 12 11 16 17 15 10
Qt 87 94 85 89 87 90 93 93 95 91 91 75 79 80 90 93
Qp 100 0 100 100 100 100 0 100 100 100 71 43 50 57 67 78
Lv 0 0 0 0 0 0 0 0 0 0 29 48 45 43 33 22
Ls 0 0 0 0 0 0 0 0 0 0 0 9 5 0 0 0
Qm 87 94 85 89 87 89 93 93 95 91 93 86 83 83 93 96
P 0 0 0 0 0 0 0 0 0 0 1 2 2 1 0 0
K 13 6 15 11 13 11 7 7 5 9 6 12 15 16 7 4
87
MCKS21 MCDII1 MCDII5 MCDI10 M (n= 20) STD.P C.L.95%
86 75 75 80 80.3 4.5 2.1
0 21 0 5 5.1 5.1 2.4
14 4 25 15 14.6 4.2 1.9
89 85 79 79 87.2 5.8 2.7
9 15 21 21 11 4.8 2.3
2 0 0 0 1.8 3.6 1.7
79 71 67 71 81.6 8.9 4.2
9 15 21 21 11 4.8 2.3
12 14 12 8 7.4 6.4 3
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
L 0 0 0 0 0 0 0 0 0 0 0 0 0 1 1 0 3 0 0 0 3 1 0 0 0 0 0 1 0 0 1 0
Qm 92 100 95 93 92 100 97 94 96 97 94 97 90 75 70 79 77 82 78 84 78 88 82 83 78 85 78 77 75 100 88 91
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Lt 8 0 5 7 8 0 3 6 4 3 6 3 10 25 30 21 23 18 22 16 22 12 18 17 22 15 22 23 25 0 12 9
80 100 100 100 86.5 18.3 8.8
20 0 0 0 12.9 17.2 8.3
0 0 0 0 0.6 1.6 0.8
90 82 76 77 88.1 5.6 2.6
1 3 1 1 0.6 0.9 0.4
9 15 23 22 11.3 5.2 2.4
Lv 0 0 0 0 0 0 0 0 0 0 0 0 0 6 5 0 12 0 0 0 12 11 0 0 0 0 0 6 0 0 10 0
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100
P 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
K 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0
A.5 Umm Ishrin Formation S.N. UI1 UI9A UI10 UI12 UI13 UI14 UI15 UI17 MCD15 MCD20 MCD23 MCD28 CR1 CR3 CR5 CR8 CR10 CR14 CR17 CR24 CR27 CR33 CR37 CR40 CR41 CR46 CR49 CR55B CR60 AK12 MCKS23 LCR22
FW 89 82 80 75 74 73 77 80 77 71 77 75 79 74 76 75 76 76 76 75 79 76 75 75 82 74 78 77 75 80 82 73
Mt 2 4 2 5 5 0 7 6 0 2 5 7 6 5 4 6 12 1 8 0 2 0 0 1 1 0 1 0 0 0 0 0
C 9 14 18 20 21 27 16 14 23 27 18 18 15 21 20 19 12 23 16 25 19 24 25 24 17 26 21 23 25 20 18 27
Qt 100 100 100 100 100 100 100 100 100 100 100 100 100 99 99 100 97 100 100 100 97 99 100 100 100 100 100 99 100 100 99 100
Qp 100 0 100 100 100 0 100 100 100 100 100 100 100 94 95 100 88 100 100 100 88 89 100 100 100 100 100 94 100 0 90 100
88
SR8 SR9 SR10 M (n= 35) STDEV.S C. l. 95%
77 82 79 77.2 3.5 1.2
4 6 3 3.0 3.0 1.0
19 12 18 19.8 4.6 1.6
100 100 100 99.7 0.8 0.3
0 0 0 0.0 0.0
0 0 0 0.3 0.8 0.3
89 95 81 87.1 8.6 3.0
0 0 0 0.0 0.0
11 5 19 12.9 8.6 3.0
100 100 100 98.1 4.0 1.4
0 0 0 1.9 4.0 1.4
0 0 0 0.0 0.0
100 100 100 100.0 0.0
0 0 0 0.0 0.0
0 0 0 0.0 0.0
C 23 21 23 23 11 8 21 25 26 25 24 25 22 15 20 24 21.0 5.2 2.8
Qt 100 100 100 100 100 100 100 100 99 99 100 99 100 100 99 100 99.7 0.4 0.2
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
L 0 0 0 0 0 0 0 0 1 1 0 1 0 0 1 0 0.3 0.4 0.2
Qm 96 96 100 97 100 78 81 72 77 80 87 76 86 86 85 81 86.1 9.1 4.8
F 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
Lt 4 4 0 3 0 22 19 28 23 20 13 24 14 14 15 19 13.9 9.1 4.8
Qp 100 100 0 100 0 100 100 100 94 100 100 94 100 100 91 100 98.5 3.1 1.5
Lv 0 0 0 0 0 0 0 0 6 0 0 6 0 0 9 0 1.5 3.1 1.5
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
Qm 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100.0 0.0
P 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
K 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
F 0 0 0 0 0 0 0 0 0 0
L 0 0 0 0 0 0 0 0 0 2
Qm 96 91 92 96 93 96 94 94 97 80
F 0 0 0 0 0 0 0 0 0 0
Lt 4 9 8 4 7 4 6 6 3 20
A.6 Disi Formation S.N. DS3 DS4 DS7 DS9 DS15 DS16 O1M4 O1M6 O1M7 O1M9 O1M19 O1M31 O1M32 O1M33 O1M34 O1M39 M (n= 16) STDEV.S C. l. 95%
FW 75 79 74 75 88 92 79 75 74 75 70 75 78 77 75 76 77.3 5.4 2.9
Mt 2 0 3 2 1 0 0 0 0 0 6 0 0 8 5 0 1.7 2.5 1.3
A.7 Umm Saham Formation S.N. US2 US3 US4 US8 US11 US12 US9B H1 H2 LOG4
FW 90 86 97 87 85 73 88 79 83 83
Mt 0 0 0 0 0 0 0 0 0 3
C 10 14 3 13 15 27 12 21 17 14
Qt 100 100 100 100 100 100 100 100 100 98
Qp 100 100 100 100 100 100 100 100 100 88
Lv 0 0 0 0 0 0 0 0 0 12
Ls 0 0 0 0 0 0 0 0 0 0
Qm 100 100 100 100 100 100 100 100 100 100
P 0 0 0 0 0 0 0 0 0 0
K 0 0 0 0 0 0 0 0 0 0
89
LOG8 LOG11 LOG15 LOG21 LOG24 LOG27 LOG30 LOG33 LOG34 LOG37 MOM0 MOM2 MOM5 MOM9 MOM11 M (n= 25) STDEV.S C. l. 95%
83 80 79 80 84 83 83 85 83 84 81 83 77 78 80 83.0 4.7 1.9
5 2 0 1 0 0 0 0 0 0 0 0 3 0 2 0.6 1.3 0.5
12 18 21 19 16 17 17 15 17 16 19 17 20 22 18 16.4 3.7 1.5
100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 99.9 0.4 0.2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.1 0.4 0.2
89 89 87 94 86 89 87 93 94 96 97 94 96 94 94 92.3 4.2 1.7
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
11 11 13 6 14 11 13 7 6 4 3 6 4 6 6 7.7 4.2 1.7
100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 99.5 2.4 1.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.5 2.4 1.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
Qt 82 82 83 89 91 77 84 95 93 86.2 6.0 4.6
F 18 18 17 11 9 23 16 5 5 13.6 6.3 4.8
L 0 0 0 0 0 0 0 0 2 0.2 0.7 0.5
Qm 82 82 83 89 91 72 80 90 91 84.4 6.4 4.9
F 18 18 17 11 9 23 16 5 5 13.6 6.3 4.8
Lt 0 0 0 0 0 5 4 5 4 2.0 2.4 1.8
Qp 0 0 0 0 0 100 100 100 100 100.0 0.0
Lv 0 0 0 0 0 0 0 0 0 0.0 0.0
Ls 0 0 0 0 0 0 0 0 0 0.0 0.0
Qm 79 82 83 89 91 75 84 95 95 85.8 7.0 5.4
P 1 0 0 0 0 3 1 0 0 0.6 1.0 0.8
K 20 18 17 11 9 22 15 5 5 13.6 6.3 4.8
Qt 86 92 93 84 90 89 90
F 14 8 7 16 10 11 10
L 0 0 0 0 0 0 0
Qm 84 88 91 84 84 85 90
F 14 8 7 16 10 11 10
Lt 2 4 2 0 6 4 0
Qp 100 100 100 0 100 100 0
Lv 0 0 0 0 0 0 0
Ls 0 0 0 0 0 0 0
Qm 86 92 93 84 90 88 90
P 0 0 0 0 0 0 0
K 14 8 7 16 10 12 10
A.8 Hiswa Formation S.N. H4 H5 H6 H7 H9 MOM15 MOM15A MOM18 MOM20 M (n= 9) STDEV.S C. l. 95%
Fw 70 73 75 76 78 77 75 86 74 76.0 4.4 3.4
Mt 14 0 25 0 3 8 0 2 0 5.8 8.6 6.6
C 16 27 0 24 19 15 25 12 26 18.2 8.7 6.7
A.9 Dubaydib Formation S.N. D1 D3 D5 D7 D8 D10 D12
FW 86 90 90 80 70 87 87
Mt 2 0 0 0 0 0 0
C 12 10 10 20 30 13 13
90
D13 D15 D17 D19 D22 D23 DMZ2 DMZ7 DMZ13 DMZ14 DMZ16 UOK0 UOK1 UOK6 UOK11 UOK15 UOK17 UOK21 UOK23 UOK25 UOK28 UOK31 UOK34 UOK35 M (n= 31) STDEV.S C. l. 95%
87 90 88 90 86 86 93 82 93 90 79 81 87 81 88 70 72 84 71 73 82 87 81 84 83.7 6.7 2.5
0 0 0 0 0 0 0 2 1 0 5 9 7 2 2 0 0 4 0 0 7 3 3 1 1.6 2.5 0.9
13 10 12 10 14 14 7 16 6 10 16 10 6 17 10 30 28 12 29 27 11 10 16 15 14.7 7.0 2.6
83 93 86 74 62 64 75 70 83 84 77 70 71 79 73 73 79 77 81 81 85 73 75 69 79.4 8.4 3.1
17 7 14 26 38 36 25 30 17 16 23 30 29 21 27 27 21 23 19 19 15 27 25 31 20.6 8.4 3.1
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
83 90 83 70 62 61 70 68 83 82 77 66 66 77 72 73 77 69 79 78 79 68 69 64 76.5 8.8 3.2
17 7 14 26 38 36 25 30 17 16 23 30 29 21 27 27 21 23 19 19 15 27 25 31 20.6 8.4 3.1
0 3 3 4 0 3 5 2 0 2 0 4 5 2 1 0 2 8 2 3 6 5 6 5 2.9 2.2 0.8
0 100 100 100 0 100 100 100 0 100 0 100 100 100 100 0 100 100 100 100 100 100 100 100 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
83 93 86 73 62 63 74 69 83 84 77 68 70 79 73 72 79 75 80 81 84 71 73 68 78.8 8.8 3.2
0 0 0 0 0 0 0 0 0 0 0 2 1 1 1 1 0 1 1 1 1 1 1 2 0.5 0.6 0.2
17 7 14 27 38 37 26 31 17 16 23 30 29 20 26 27 21 24 19 18 15 28 26 30 20.7 8.5 3.1
F 17 27 20 24 16 28 16 9 19 21 21 24 26 14
L 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 76 71 75 70 82 71 81 83 77 75 77 74 71 81
F 17 27 20 24 16 28 16 9 19 21 21 24 26 14
Lt 7 2 5 6 2 1 3 8 4 4 2 2 3 5
Qp 100 100 100 100 100 100 100 100 100 100 100 100 100 100
Lv 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Ls 0 0 0 0 0 0 0 0 0 0 0 0 0 0
Qm 82 72 79 74 84 72 84 91 80 78 78 75 73 85
P 0 0 0 0 0 1 1 0 0 0 0 0 0 0
K 18 28 21 26 16 27 15 9 20 22 22 25 27 15
A.10 Mudawwara Formation S.N. TB1 TB5 TB7 TB9 TB11 LS2 LS8 LS11 AM1 AM2 AM4 AM9 BT1 BT4
FW 89 91 86 94 87 82 74 82 77 75 89 90 90 74
Mt 0 0 0 0 0 2 0 1 20 0 0 0 0 3
C 11 9 14 6 13 16 26 17 3 25 11 10 10 23
Qt 83 73 80 76 84 72 84 91 81 79 79 76 74 86
91
LS16 LS18 LS20 LS24 RS1 RS3 RS5 RS6 RS8 RS9 RS10 LS30 LS32 LS34 LS36 LS45 LS48 M (n= 31) STDEV.S Conf.l.95
87 86 87 78 70 74 75 70 76 75 75 81 84 87 89 88 74 81.8 7.0 2.6
0 1 0 6 12 4 5 2 2 3 2 3 1 1 0 2 0 2.3 4.1 1.5
13 13 13 16 18 22 20 28 22 22 23 16 15 12 11 10 26 15.9 6.4 2.3
84 72 84 72 72 75 67 77 78 75 72 88 81 72 85 76 71 78.0 5.9 2.2
16 28 16 28 28 25 33 23 22 25 28 12 19 28 15 24 29 22.0 5.9 2.2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
82 72 82 69 70 71 65 77 74 74 72 84 81 72 75 70 71 75.0 4.9 1.8
16 28 16 28 28 25 33 23 22 25 28 12 19 28 15 24 29 22.0 5.9 2.2
2 0 2 3 2 4 2 0 4 1 0 4 0 0 10 6 0 3.0 2.5 0.9
100 0 100 100 100 100 100 0 100 100 0 100 100 100 100 100 0 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
84 72 84 71 71 74 67 77 77 75 72 87 80 70 83 74 71 77.3 5.9 2.2
1 1 0 0 0 0 0 0 0 0 0 0 0 1 1 1 0 0.2 0.4 0.1
15 27 16 29 29 26 33 23 23 25 28 13 20 28 16 25 29 22.5 5.9 2.2
C 9 10 12 16 12 12 16 12.4 2.7 2.5
Qt 83 84 85 81 77 79 80 81.3 2.9 2.7
F 17 16 15 19 23 21 20 18.7 2.9 2.7
L 0 0 0 0 0 0 0 0.0 0.0
Qm 83 84 85 80 72 77 78 79.9 4.6 4.3
F 17 16 15 19 23 21 20 18.7 2.9 2.7
Lt 0 0 0 1 5 2 2 1.4 1.8 1.7
Qp 0 0 0 100 100 100 100 100.0 0.0
Lv 0 0 0 0 0 0 0 0.0 0.0
Ls 0 0 0 0 0 0 0 0.0 0.0
Qm 83 84 85 80 76 79 79 80.8 3.2 3.0
P 0 0 0 1 1 0 0 0.3 0.5 0.5
K 17 16 15 19 23 21 21 18.9 3.0 2.8
C 10 9
Qt 100 100
F 0 0
A.11 Khusha Formation S.N. KH1 KH2 KH4 S1 S6 S12 S15 M (n= 7) STDEV.S C. l. 95%
FW 91 90 88 80 88 88 84 87.0 3.8 3.5
Mt 0 0 0 4 0 0 0 0.6 1.5 1.4
A.12 Kurnub Group S.N. CrM in CrK2
FW 90 91
Mt 0 0
L 0 0
Qm 98 100
F 0 0
Lt 2 0
Qp 100 0
Lv 0 0
Ls 0 0
Qm 100 100
P 0 0
K 0 0
92
CrK7 CrZ2 CrZ4 CrZ9 CrZ11 CrZ18 CrZ22 CrZ23 CrZ27 CrZ28 CrZ36 CrZ39 CrZ48 CrD5 CrD12 CrD16 CrD19 CrD24 TB13 BT10 K1 KN1 KN3 KN6 R4 R9 M (n= 28) STDEV.S C. l. 95%
78 84 82 78 90 82 84 91 76 81 71 96 73 93 75 74 85 95 87 88 80 88 91 81 90 88 84.4 7.0 2.7
15 0 0 12 0 2 0 0 0 5 1 0 0 0 20 12 6 5 8 6 12 1 2 3 0 11 4.3 5.6 2.2
7 16 18 10 10 16 16 9 24 14 28 4 27 7 5 14 9 0 5 6 8 11 7 16 10 1 11.3 7.0 2.7
100 100 100 96 100 100 100 100 100 100 98 100 98 100 100 100 100 100 100 100 100 100 100 100 100 100 99.7 0.9 0.3
0 0 0 4 0 0 0 0 0 0 2 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0.3 0.9 0.3
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
100 93 99 95 94 98 99 97 92 96 96 96 94 97 91 94 95 97 95 100 95 98 98 95 98 94 96.2 2.4 0.9
0 0 0 4 0 0 0 0 0 0 2 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0.3 0.9 0.3
0 7 1 1 6 2 1 3 8 4 2 4 4 3 9 6 5 3 5 0 5 2 2 5 2 6 3.5 2.4 0.9
0 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 100 0 100 100 100 100 100 100 100.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
100 100 100 96 100 100 100 100 100 100 98 100 99 100 100 100 100 100 100 100 100 100 100 100 100 100 99.7 0.0
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0.0 0.0
0 0 0 4 0 0 0 0 0 0 2 0 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0.3 0.0
93
Graphical abstract
94
Highlights
The study investigates part of the vast N Gondwana lower Paleozoic sandstone sheet It evaluates petrographically the factors governing modal composition of sandstone Provenance controlled by plate tectonics appears to be the primary factor About 50% of the siliciclastic sequence represents a success for Dickinson‘s approach Intracratonic syn-rift extrusion or glacial effects are behind its inapplicability