Tepee structures and associated diagenetic features in intertidal carbonate sands (lower Jurassic, Morocco)

Burri, P.; Dresnay, Renaud du; Wagner, C. W.

doi:10.1016/0037-0738(73)90046-8

Cited by 38 publications

(13 citation statements)

References 2 publications

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“…Flooding of these sediments by hypersaline marine water was resulted in the deposition of flowstone, spheroids, hemispheroids, and giant aragonite ray-crystals in the fenestrae and as crusts in the sabkha sequence. Similar paleoflowstone were reported in Permian lime stones of New Mexico ("stromatactis" of Otte and Parks, 1963), in Triassic rocks from Aus tria (Zankl, 1971) and from Jurassic tepee struc tures in Morocco (Burri et al, 1973) and were interpreted as organic crusts.…”

Section: Diagenetic Modelssupporting

confidence: 71%

Some diagenetic fabrics of aragonite, calcite and native sulfur in the Miocene evaporite cycle on the Red Sea coast, Egypt.

Sayed

Youssef

1989

J. Min. Petr. Econ. Geol.

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The fabrics and presence of celestite in the carbonate cements in the reefal limestone of Gebel El Rusas Formation and the sabkha sequences of the Abu Dabbab Formation (Middle Miocene) suggest deposition in a hypersaline vadose regime. The recorded carbonate cements are re presented by paleoflowstone crusts; spheroidal and hemispheroidal structures and giant plaeo aragonite ray-crystals deposited in fenestrae and as crusts within the Miocene sediments.The carbonate cements occur in the form of polycrystalline calcite pseudospar and fibrous calcite resulting from paramorphic replacement of aragonite in Mg-poor fresh water vadose regime. Traces of native sulfur is formed together with secondary gypsum and calcite in the surficial layer of the Abu Dabbab evaporites. It is formed in a localized microenvironment in the fresh water vadose regime due to bacterial activity on sulfate deposits.

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Section: Diagenetic Modelssupporting

confidence: 71%

Some diagenetic fabrics of aragonite, calcite and native sulfur in the Miocene evaporite cycle on the Red Sea coast, Egypt.

Sayed

Youssef

1989

J. Min. Petr. Econ. Geol.

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“…Hardground structures resembling those described here have been recorded as tepee structures or pseudo-anticlines (e.g. Shinn, 1969;Assereto & Kendall, 1971, 1977Burri, Du Dresnay & Wagner, 1973;Evamy, 1973). Most of them originated under subaerial exposure (peritidal tepee structures, caliche pseudo-anticlines) as buckled margins of saucer-like megapolygons.…”

Section: Discussionsupporting

confidence: 56%

Development of relief on a Middle Jurassic cemented sea floor: origin of submarine pseudo‐anticlines in the Bathonian of Normandy

Fürsich

Palmer

1979

Sedimentology

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On the foreshore east of Luc‐sur‐Mer, Normandy, an Upper Bathonian hard‐ground which caps a sponge biostrome has been thrown into a series of troughs and ridges, the latter sometimes with very steep flanks. Faunal orientation and encrustation of extensive undercuts demonstrate that these structures are of a syn‐sedimentary origin. They are interpreted as submarine pseudo‐anticlines which have a composite origin. The following three factors are thought to have contributed to their formation: (a) a primary morphological differentiation of the underlying biostrome; (b) sediment expansion caused by force of crystallization during hardground formation; and (c) differential compaction, being greater where the hardground overlies mainly inter‐reef mud as compared with the rigid sponge framework. The main episode of this compaction occurred at an early stage in the life of the hardground. Subsequent erosion, colonization by encrusters and borers, and burial beneath a fossiliferous clay were the final stages in the history of these pseudo‐anticlines.

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“…These include those of the Jurassic of Morocco ( Fig. 9) (Burri, DuDresnay & Wagner, 1973), the Triassic of the Italian Alps (Assereto & Kendall, 1977), the Permian of the Guadalupe Mountains in the United States ( Fig. 10) (Assereto & Kendall, 1977) and the Lower Proterozoic Rocknest Dolomite of Northwest Canada (Grotzinger & Read, 1983).…”

Section: Peritidal Tepees Their Crusts Their Cements and Related mentioning

confidence: 99%

“…These crusts formed at the depositional surface and apparently continued accumulating during early burial. Examples of these cements can be seen in the Lower Proterozoic Wopney Orogen, Canada (Grotzinger & Read, 1983), the Devonian of the Canning basin, Western Australia (Playford, private communication), the Permian of the Guadal-upe Mountains Assereto & Kendall, 1977;Warren 1983a;Rosenblum, 1985), the Triassic of the Italian Alps (Assereto & Kendall, 1977) and the Jurassic of the Moroccan High Atlas Mountains (Burri et al, 1973;Assereto & Kendall, 1977). Such marinevadose and marine-phreatic travertines frequently fill the fractures and cavities in the deformed compressional ridges found in these crusts, and these deformed crusts are commonly composed of coated grains and/ or pisolites (Fig.…”

Section: Peritidal Tepees Their Crusts Their Cements and Related mentioning

confidence: 99%

A review of the origin and setting of tepees and their associated fabrics

1987

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Carbonate hardgrounds often occur at the surface of shallow subtidal to supratidal, lacustrine, and subaerial carbonate shelf sediments. These are commonly disrupted and brecciated when the surface area of these crusts increases. In the subtidal environment, megapolygons form when cementation of the matrix causes the surface area of the hardgrounds to expand. Similar megapolygons form in the supratidal, lacustrine and subaerial settings when repeated incremental fracturing and fracture fill by sediment and/or cement also causes the area of the hardgrounds to expand. The arched up antiform margins of expansion megapolygons are known as tepees. The types of tepees found in the geological record include: (1) Submarine tepees which form in shallow carbonate‐saturated waters where fractured and bedded marine grainstones are bound by isopachous marine‐phreatic acicular and micritic cements. The surfaces of these brecciated crusts have undergone diagenesis and are bored. Unlike tepees listed below they contain no vadose pisolites or gravity cements; (2) Peritidal and lacustrine tepees are formed of crusts characterized by fenestral. pisolitic and laminar algal fabrics. This similarity in fabric makes these tepees of different origins difficult to separate. Peritidal tepees occur where the marine phreatic lens is close to the sediment surface and the climate is tropical. They are associated with fractured and bedded tidal flat carbonates. Their fracture fills contain geopetal asymmetric travertines of marine‐vadose origin and/or marine phreatic travertines and/or Terra rossa sediments. The senile form of these peritidal tepees are cut by labyrinthic dissolution cavities filled by the same material. Lacustrine tepees form in the margins of shallow salinas where periodic groundwater resurgence is common. They include groundwater tepees which form over evaporitic ‘boxwork’ carbonates, and extrusion tepees which also form where periodic groundwater resurgence occurs at the margins of shallow salinas, but the dominant sediment type is carbonate mud. These latter tepee crusts are coated and crosscut by laminated micrite; the laminae extend from the fractures downward into the underlying dolomitic micrite below the crust. Both peritidal and lacustrine tepees form where crusts experience alternating phreatic and vadose conditions, in time intervals of days to years. Cement morphologies reflect this and the crusts often contain gravitational, meniscus vadose cements as well as phreatic isopachous cement rinds. (3) Caliche tepees which are developed within soil profiles in a continental setting. They are formed by laminar crusts which contain pisolites, and fractures filled by micritic laminae, microspar, spar and Terra rossa. Most of the cements are gravitational and/or meniscoid. In ancient carbonates, when their cementation and diagenetic fabric can be interpreted, tepee structures can be used as environmental indicators. They can also be used to trace the evolution of the depositional and hydrological setting.

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Tepee structures and associated diagenetic features in intertidal carbonate sands (lower Jurassic, Morocco)

Cited by 38 publications

References 2 publications

Some diagenetic fabrics of aragonite, calcite and native sulfur in the Miocene evaporite cycle on the Red Sea coast, Egypt.

Some diagenetic fabrics of aragonite, calcite and native sulfur in the Miocene evaporite cycle on the Red Sea coast, Egypt.

Development of relief on a Middle Jurassic cemented sea floor: origin of submarine pseudo‐anticlines in the Bathonian of Normandy

A review of the origin and setting of tepees and their associated fabrics

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