Pisoids and Pisolite Facies (Permian), Guadalupe Mountains, New Mexico and West Texas

Esteban, Mateu; Pray, Lloyd C.

doi:10.1007/978-3-642-68869-0_43

Cited by 39 publications

(25 citation statements)

References 14 publications

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“…Assereto and Folk (1976) and Loucks and Folk (1976) concluded that the pisoids were produced by marginal marine supratidal environments. Intensive research by Lloyd Pray and his group led to a complete rejection of the caliche and the vadose origin hypotheses (Esteban andPray 1976, 1983). The authors interpreted the pisoid depositional setting as a shelf crest of a carbonate marginal mound separating an evaporitic lagoon from a more open-marine area.…”

Section: Economic Importancementioning

confidence: 98%

“…brick-like textures or elongated rays with square termination interpreted as aragonite relicts formed in hypersaline settings (Assereto and Folk 1976;Esteban 1976;Esteban and Pray 1983;Chafetz and Butler 1980;Hay and Wiggins 1980). Caliche pisoids originate in situ at the surface or within surface layers by evaporation.…”

Section: Modern Pisoids: Environments and Controlsmentioning

confidence: 98%

“…Caliche pisoids, cave pisoids, lacustrine pisoids and meteoric-vadose and marine-vadose pisoids can be used to recognize different subenvironments of terrestrial and marginal marine settings (Esteban and Pray 1983). Standard microfacies 25 underlines the importance of pisolitic carbonate rocks.…”

Section: Depositional Settingsmentioning

confidence: 99%

“…The light laminae consist of microspar. Dark laminae are interpreted as microbially induced (Esteban andPray 1983, Jones andMacDonald 1989). The number of laminae is variable and ranges from distinctly more than in ooids to only few.…”

Section: Shapementioning

confidence: 99%

“…Vadoid is a useful term if the vadose origin is sufficiently substantiated. A specific variety of pisoids, first recognized in back-reef strata of the Permian Reef Complex in New Mexico and West Texas, has been called walnutoid (Esteban and Pray 1983;Pl. 34/6, Pl.…”

Section: Terminologymentioning

confidence: 99%

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Microfacies Data: Matrix and Grains

Flügel

2009

Microfacies of Carbonate Rocks

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MicrofabricGrain size: Is measured by counting the longest diameter of 100 to 200 grains. Allows attribution to grain size-based classifications. 'Sorting' in micrites, as the result of competition between space and grain growth, can be used as measure of the textural maturity of fine-crystalline carbonates. Grain size ranges may reflect differences in the depositional environment (e.g. reef micrites and micrites in limestone/shale sequences). Differences in predominant crystal sizes provide indications of the potential aragonite-dominated or calcite-dominated precursors of calcite micrites. Grain contacts: Grain contacts seen under the SEM are straight, curvilinear or serrate. The percentage of specific grain contacts reflects the degree of diagenetic changes (e.g. recrystallization). Grain shape: Differentiation of anhedral, subhedral and euhedral micrite grains. Anhedral and subhedral grains forming a hypidiotopic fabric appear to be common in micritic rocks composed of grains > 4 μm. Irregular, interlocked grains form an 'amoeboid mosaic', in contrast to block-like grains forming a 'pavement mosaic' common in limestones affected by thermal stress. Most micrite grains are angular to subangular. Subrounded and rounded grains result from intergranular solution and crystal overgrowth. Inclusions in crystals: Liquid and gas inclusion pits are common in microspar crystals as well as in larger spar crystals.The composition of the inclusions indicates the conditions under which recrystallization took place. Microfenestrae: Some micrites contain round voids, 40 to 80 μm in size, which are filled with blocky calcite. The preservation of this microfenestral fabric is used as evidence against a strong mechanical compaction of the sediment prior to lithification. Boundary between calcite matrix and fossils: Diagenetic stages are distinguished by differences in the boundaries between matrix and fossils: (a) Sharp boundaries between matrix and Low-Mg calcite fossils (e.g. brachiopods, bryozoans, ostracods, trilobites) with well-preserved ultrastructures; (b) moderately sharp boundaries between matrix and fossils (recrystallized tabulate and rugose corals, stromatoporoids); and (c) boundaries between matrix and fossils (e.g. mollusks) which are difficult to recognize. Microporosity: SEM studies reveal numerous types of micropores (5-10 μm wide) in micritic limestones, including both primary and solution-enhanced intercrystalline pores, as well as micromolds, microvugs and microchannels (Pl. 7/6; see Chap. 5). Microporosity is developed in many subsurface micritic limestones, including significant petroleum reservoirs in Mesozoic and Tertiary deposits of the Middle East, North Africa, and the North American Gulf Coast. Skeletal grainsA main advantage of SEM studies of micrites is the possibility of recognizing the occurrence and abundance of planktonic nannofossils (Pl. 7/3-5, Pl. 77/23) in mudstones and wackestones in both deep-water and shallow-water settings. SEM differentiation of silt-sized and smaller bioclastic grains ...

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Section: Economic Importancementioning

confidence: 98%

Section: Modern Pisoids: Environments and Controlsmentioning

confidence: 98%

Section: Depositional Settingsmentioning

confidence: 99%

Section: Shapementioning

confidence: 99%

Section: Terminologymentioning

confidence: 99%

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