Ramp reef depositional facies model for the Mid-Pliocene Golden Gates Reef Member of the Tamiami Formation, South Florida

Meeder, John F.; Klaus, James S.; Grasmueck, Mark

doi:10.1007/s10347-019-0582-3

Cited by 4 publications

(4 citation statements)

References 42 publications

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“…Dissolution in the studied carbonates resulted in the development of several types of pores, including intergranular, moldic, and vuggy porosity (Figure 7e). Dissolution process of the metastable minerals has been followed by precipitation of calcite in dissolved parts and among grains (Figure 7f) (Meeder, Klaus, & Grasmueck, 2019). The filling of biomoldic porosity by blocky and drusy cements suggests diagenesis in the meteoric phreatic setting (Longman, 1980).…”

Section: Resultsmentioning

confidence: 99%

Facies analysis and sequence stratigraphy of the Middle Miocene Marmarica Formation at Siwa area, north Western Desert, Egypt

et al. 2022

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The Middle Miocene rocks in the northern part of the Western Desert of Egypt are dominated by carbonate rocks that constitute the Marmarica Formation. To determine the depositional environments and sequence architecture of the Marmarica Formation, three sections were described and sampled in detail. These sections from west to east are; Girba, Naqb El‐Migahhiz, and Gabal Umm Hiyus. The Marmarica Formation in the Siwa area includes three members, from bottom to top: the Oasis, Siwa Escarpment, and El Diffa Plateau members. The microfacies of the Marmarica Formation comprise abundant mud‐supported microfacies with minor grain‐supported microfacies. Sedimentation during the Middle Miocene took place on a homoclinal ramp. Dolomitization is the most prevalent diagenetic process that affected carbonate sediments of the Marmarica Formation. The Marmarica Formation comprises two sequence boundaries. The first sequence boundary (SB1) is demarcated by the presence of Thalassinoides ichnofacies at the boundary between the Oasis and Siwa Escarpment members in all the studied sections. It is considered a type 1 sequence boundary. The second sequence boundary (SB2) is represented by an erosional surface, which is recorded only in Girba section. The SB2 was traced at both Naqb El‐Migahhiz and Umm Hiyus sections by the occurrence of burrows that relate to the Glossifungites ichnofacies. The latter boundary is considered type 2. Three third‐order depositional sequences have been recognized in the Middle Miocene Marmarica Formation. Therefore, the Marmarica Formation at Siwa Oasis exhibits relative sea‐level oscillation. During the Middle Miocene, the prevailing warm climate caused transgression and deposition of carbonates along the marine shelf surrounding western and northern Africa.

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Section: Resultsmentioning

confidence: 99%

Facies analysis and sequence stratigraphy of the Middle Miocene Marmarica Formation at Siwa area, north Western Desert, Egypt

et al. 2022

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“…), fine nodular phosphate, grey Limestone, wackestone Supratidal (Gomez & Astini, 2015;Shinn, 1983) B/A T Tamiami Formation Limestone, wackestone, moderately hard, laminations, sandy Calcitic shell with fine quartz sand Intertidal (Gebelin, 1977;Sussko & Davis, 1992) A/K Tamiami Formation Unconsolidated calcitic shell with up to 40% very fine grained quartz sand. May contain small, oyster fragments, grey Quartz sand with trace of sand-sized skeletal fragments Intertidal (Gomez & Astini, 2015;Shinn, 1983) A/J Tamiami Formation Unconsolidated quartz sand, fine to very fine, dark brownish grey, organics Limestone, wackestone, intraclasts, sandy Supratidal (Hardie, 1977;(Hardie & Shinn, 1988;Missimer, 1970) A/I Tamiami Formation Limestone, wackestone, moderately indurated, intraclasts Unlithified, quartz sand and shell Shallow offshore, shelf (Meeder, 1987;Zeller et al, 2015) C/C (Meeder, 1987;Perkins, 1977) C/C D Caloosahatchee Formation Predominantly sandy skeletal wackestone, some packstone, distribution of quartz sand highly variable…”

Section: Caloosahatchee Formationmentioning

confidence: 99%

“…Unlithified quartz sand and shell Beach or very proximal subtidal (offshore) (Allmon, 1992) C/C C Caloosahatchee Formation Numerous mollusc types, no mud, may be death assemblage Sandy molluscan wackestone Offshore, shallow shelf (Holmes, 1988;Meeder, 1987) C/C B Caloosahatchee Formation Sandy wackestone, variable composition with sand shell, and mud, not proximal to beach, but shallow water Sandy wackestone/ packstone Discontinuity crust, onshore (Gerdes & Krumbein, 1987;Goudie, 1973;Multer & Hoffmeister, 1968) C/C A Caloosahatchee Formation Sandy wackestone/packstone, sandstone in place, very hard, some laminations of quartz sand and mud Sandy, wackestone, freshwater Interior wetland marl (Pederson et al, 2019) B/80 east base Fort Thompson, Formation Sandy wackestone, lime mud with freshwater molluscs, slightly sandy…”

Section: Caloosahatchee Formationmentioning

confidence: 99%

A Plio‐Pleistocene eustatic and storm‐controlled mixed carbonate–siliciclastic marine ramp deposit in south‐west Florida: An example of sediment homogenisation with maintenance of carbonate‐producing organisms

Missimer

Hegy

2023

The Depositional Record

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Mixed siliciclastic and carbonate sediments are common in the stratigraphic record, but fully homogenised mixes are not. Many occurrences of mixed sediment sequences are dominated by end‐members with stacking of ‘nearly pure’ lithfacies (e.g. cyclothems containing alternating sandstone, limestone and coal units). The Plio‐Pleistocene sediments within south‐west Florida provide insights into the occurrence of fully homogenised siliciclastic/carbonate deposits. In all defined environments from lagoon to supratidal to inner tidal to beach to offshore to coral reef, quartz sand coexists with carbonates. Perhaps the key feature that allowed full homogenisation of the sediments within all facies and subfacies was the relatively shallow water (<10 m), which facilitated mixing during low‐order eustatic sea‐level events and storms. However, four factors contributed to the full homogenisation of the sediment types without termination or inhibition of carbonate organism growth. These factors are (1) the shallow water allowing wave‐driven sediment transport (all environments within the wave orbital depth), (2) close proximity and perhaps irregular nature of the depositional environment boundaries, (3) low influx rate of quartz sand via longshore transport, and (4) the lack of significant terrigenous mud transport into the system. Mixing processes at the large‐scale included movement of sediments from one depositional environment to another during storms, mixing along facies boundaries, and in situ mixing within autochthonous and parautochthonous mollusc death assemblages. At the smaller scale, mixing occurred by bioturbation and diagenetic dissolution of carbonate skeletal grains during minor high sea‐level stands.

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“…Since then, Hunter (1968) subdivided the Tamiami Formation into five members: the Ochopee Limestone Member, Buckingham Limestone Member, Pinecrest Sand Member, Murdock Station Member, and the Bayshore Clay Member. A sixth member, the Golden Gate Reef Member, was later described by Meeder (1979). This entire sequence of the Tamiami Formation was constrained to an age of 4.95 to 1.95 Ma via strontium isotopic geochronology (Missimer, 1992), which encompasses almost all of the Pliocene as well as the early Pleistocene.…”

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confidence: 99%

The first documented fossil records of Isistius and Squatina (Chondrichthyes) from Florida, with an overview of the associated vertebrate fauna

Perez,

Marks

2017

FLMNH

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In October 2016, an email inquiring about the geologic age of a creek in Sarasota County led to the serendipitous ‘discovery’ of fossil teeth of the sharks Isistius triangulus and Squatina sp. in Florida. Up to that point, no fossils of Isistius or Squatina from Florida were present in the vertebrate paleontology collections at the Florida Museum of Natural History, nor had they been listed in any scientific publication. However, public inquiries revealed that the presence of both genera in the Florida fossil record has been known among the amateur paleontology community for well over a decade. Once co-author Marks was made aware that the Isistius teeth represented something novel, more rigorous collecting was conducted to procure more specimens. A total of 94.5 kg of matrix from four gravel deposits within the creek, informally known as Cookiecutter Creek, were screenwashed and picked to produce 186 whole or partial lower teeth of Isistius triangulus and four teeth belonging to Squatina. In addition, a diverse vertebrate fauna was recovered that ranged from Pliocene to Pleistocene in age. Screenwashing of 7.5 kg of matrix from the in situ Pleistocene Caloosahatchee Formation revealed no specimens of Isistius or Squatina, which implies their actual source is the underlying Pliocene Tamiami Formation. The unprecedented occurrence of Isistius triangulus, with such a high density in Cookiecutter Creek relative to other sites in Florida, may indicate that Cookiecutter Creek preserves a unique deep-water facies within the Tamiami Formation. The associated vertebrate fauna includes taxa from marine, brackish, freshwater, and fully terrestrial paleoenvironments; providing evidence of local sea-level fluctuations during the Pliocene to Pleistocene. The temporally mixed accumulation in these gravel deposits inhibits a more accurate reconstruction of these sea-level fluctuations.

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Ramp reef depositional facies model for the Mid-Pliocene Golden Gates Reef Member of the Tamiami Formation, South Florida

Cited by 4 publications

References 42 publications

Facies analysis and sequence stratigraphy of the Middle Miocene Marmarica Formation at Siwa area, north Western Desert, Egypt

Facies analysis and sequence stratigraphy of the Middle Miocene Marmarica Formation at Siwa area, north Western Desert, Egypt

A Plio‐Pleistocene eustatic and storm‐controlled mixed carbonate–siliciclastic marine ramp deposit in south‐west Florida: An example of sediment homogenisation with maintenance of carbonate‐producing organisms

The first documented fossil records of Isistius and Squatina (Chondrichthyes) from Florida, with an overview of the associated vertebrate fauna

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