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Journal Article

BATHYSIPHON (FORAMINIFERIDA) AT PACHECO PASS, CALIFORNIA: A GEOPETAL, PALEOCURRENT, AND PALEOBATHYMETRIC INDICATOR IN THE FRANCISCAN COMPLEX

DAVID B. SAJA, HERMANN W. PFEFFERKORN, STEPHEN P. PHIPPS
Journal: PALAIOS
Published: 01 March 2009
PALAIOS (2009) 24 (3): 181–191.
DOI: https://doi.org/10.2110/palo.2008.p08-037r
.... Bathysiphon specimens can be used as geopetal indicators, since they occur parallel to bedding at the top of argillaceous layers, as paleocurrent indicators (showing a SSE trend at Pacheco Pass), and as paleobathymetric indicators, suggesting, by their large size, mid-to-lower bathyal depths (2000–4000 m...
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View PDF for article title, BATHYSIPHON (FORAMINIFERIDA) AT PACHECO PASS, CALIFORNIA: A <span class="search-highlight">GEOPETAL</span>, PALEOCURRENT, AND PALEOBATHYMETRIC INDICATOR IN THE FRANCISCAN COMPLEX
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Book Chapter

Geopetal Fabrics

Author(s)
Peter A. Scholle
Book: A Color Illustrated Guide to Carbonate Rock Constituents, Textures, Cements, and Porosities
Series: AAPG Memoir
Publisher: American Association of Petroleum Geologists
Published: 01 January 1978
DOI: 10.1306/M27394C29
EISBN: 9781629811994
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Journal Article

Shrunken (geopetal) ooids; evidence of origin unrelated to carbonate-evaporite diagenesis

S. J. Mazzullo
Published: 01 March 1977
Journal of Sedimentary Research (1977) 47 (1): 392–397.
DOI: https://doi.org/10.1306/212F7180-2B24-11D7-8648000102C1865D
...S. J. Mazzullo Abstract The presence of shrunken ooids is thought to be related to the former presence of evaporites in associated rocks. Geopetal ooid textures which resemble shrunken ooids were observed in Cambrian carbonates from the Mohawk Valley of New York in which no evidence of former...
View PDF for article title, Shrunken (<span class="search-highlight">geopetal</span>) ooids; evidence of origin unrelated to carbonate-evaporite diagenesis
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Journal Article

Positive-relief bedforms on modern tidal flat that resemble molds of flutes and grooves; implications for geopetal criteria and for origin and classification of bedforms

Gerald M. Friedman, John E. Sanders
Published: 01 March 1974
Journal of Sedimentary Research (1974) 44 (1): 181–189.
DOI: https://doi.org/10.1306/74D729B9-2B21-11D7-8648000102C1865D
View PDF for article title, Positive-relief bedforms on modern tidal flat that resemble molds of flutes and grooves; implications for <span class="search-highlight">geopetal</span> criteria and for origin and classification of bedforms
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Journal Article

Geopetal Fabrics: Important Aids for Interpreting Ancient Reef Complexes: ABSTRACT

P. E. Playford, A. E. Cockbain
Journal: AAPG Bulletin
Published: 01 March 1972
AAPG Bulletin (1972) 56 (3): 645.
DOI: https://doi.org/10.1306/819A3FE2-16C5-11D7-8645000102C1865D
...P. E. Playford; A. E. Cockbain Abstract The term “geopetal fabric” was introduced by Sander for fabrics in sedimentary rocks “which record the direction of the earth’s surface at the time they were being formed.” Geopetal fabrics thus can be used to determine the orientation of these rocks ( i.e...
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Journal Article

Geopetal pyrite in fine-grained limestones

S. Honjo, A. G. Fischer, R. Garrison
Published: 01 June 1965
Journal of Sedimentary Research (1965) 35 (2): 480–488.
DOI: https://doi.org/10.1306/74D712B2-2B21-11D7-8648000102C1865D
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Image
Plane polarized photomicrographs of geopetal sediment in Owl Olistolith (up direction noted by arrows). A) GO-18, all geopetal sediment is oriented the same direction. B) GO-5, geopetal sediment with two different orientations, which confirms that the olistolith is no longer in its original position.

Plane polarized photomicrographs of geopetal sediment in Owl Olistolith (up...

Published: 21 November 2022
Fig. 11 Plane polarized photomicrographs of geopetal sediment in Owl Olistolith (up direction noted by arrows). A ) GO-18, all geopetal sediment is oriented the same direction. B ) GO-5, geopetal sediment with two different orientations, which confirms that the olistolith is no longer in its
Image
- Drowning succession at Carito: a,b) brachiopod-rich facies with geopetal structures (upper Pliensbachian); c) thin section view of the brachiopod-rich facies; d) packstone with small gastropods (G), ammonites (A), echinoderms (E), sponge spicules (SS) and various undetermined benthic material; e) pack/wackestone with a large ammonite and abundant “Posidonia” bivalves; f) close-up of silicified aptychi (scale bar 0.5 mm).

- Drowning succession at Carito: a,b) brachiopod-rich facies with geopetal ...

Published: 01 February 2020
Fig. 6 - Drowning succession at Carito: a,b) brachiopod-rich facies with geopetal structures (upper Pliensbachian); c) thin section view of the brachiopod-rich facies; d) packstone with small gastropods (G), ammonites (A), echinoderms (E), sponge spicules (SS) and various undetermined benthic
Image
Geopetal structures in oriented drill core from Prominent Hill indicate that Cu-rich sulfide mineralization occurred after tilting of the host rocks to a steep orientation. (A). Hematite-sericite ± chlorite-altered graywacke showing cavity with sericite-altered wall-rock debris and Cu sulfides at bottom (yellow arrows), and late calcite infill; PH07D313, 569.4m. (B). Hematite-quartz-altered sandstone showing cavity partly filled with altered sandstone debris followed by deposition of two calcite generations separated by fine-grained hematite and Cu sulfide precipitations 1 and 2 (yellow arrows); PH05D160, 402.1m. (C). Combined transmitted and reflected light image (left) and normal photo (right) of hematite quartz-altered sandstone with cavity filled by wall-rock debris of generation 1 (white arrows) and calcite; sandstone clasts are rimmed by calcite (gray) followed by bornite, hematite, (yellow arrow), and later infill of barite (transparent); PH05D130, 615.4m. Mineral abbreviations: Bn = bornite, Cal = calcite, Cc = chalcocite.

Geopetal structures in oriented drill core from Prominent Hill indicate tha...

Published: 01 December 2015
Fig. 13 Geopetal structures in oriented drill core from Prominent Hill indicate that Cu-rich sulfide mineralization occurred after tilting of the host rocks to a steep orientation. (A). Hematite-sericite ± chlorite-altered graywacke showing cavity with sericite-altered wall-rock debris and Cu
Image
(A) Geopetal textures in vertically oriented rock slab, Ada Edith claims, Nevada. A dark fine-grained dolomite forms a layer at the base of solution cavities. Coarse-grained white dolomite fills the upper part of the cavity. Solution cavities vary in shape, from irregular to rounded in outline. (B) Geopetal texture in solution cavity in vertically oriented rock slab, Rose mine, Nevada. Solution cavities filled by two types/generations of dolomite are common at HZD localities. (C) Dark, fine-grained dolomite lines the base of white, coarse-grained layers, forming a geopetal fabric, Cedar Peak, Nevada. (D) Microbreccia fills a topographic low and lines the top of a gray layer. Dissolution and solution collapse of the upper gray layer contributed the microbreccia material that forms the geopetal fabric. The microbreccia is cemented by the later coarse-grained saddle dolomite.

(A) Geopetal textures in vertically oriented rock slab, Ada Edith claims, N...

Published: 01 October 2010
Figure 7. (A) Geopetal textures in vertically oriented rock slab, Ada Edith claims, Nevada. A dark fine-grained dolomite forms a layer at the base of solution cavities. Coarse-grained white dolomite fills the upper part of the cavity. Solution cavities vary in shape, from irregular to rounded
Image
Photographs of calc-silicate xenoliths, sheeting, enclaves, and geopetal structures. (A) Fine-grained (pale gray) syenitic sheets with bulbous contacts with white, coarse-grained syenitic host on their east sides and subplanar contacts on their western sides. View to north-northwest at Groningen (syenite zone). Hammer is 59 cm long. (B) Sheeting in the diorite zone along the western shore of Burøya. Thin (0.5–1-m-wide) dioritic dikes are separated by centimeter- to decimeter-scale syenitic stringers. (C) A south-facing outcrop on southern Kleppan (sheeted zone) shows a sequence of four west-dipping dioritic sheets. Three of the dioritic sheets are separated from one another by white syenite, which has flame-like structures penetrating eastward into the diorite. Also note the bulbous zones along the western side of the two central dioritic sheets. The flame structures and bulbous zones (load casts) indicate that original “up” direction was to the east in modern coordinates and that the sheets are overturned (see text). Pallet in foreground is ~1 m wide. (D) Blocky calc-silicate xenoliths in a dioritic sheet in the eastern part of the complex; from Svartskjæret (eastern zone). Hammer is 38 cm long. (E) Gray dioritic pillows in white syenite; from Langdraget (eastern zone). Hammer is 38 cm long.

Photographs of calc-silicate xenoliths, sheeting, enclaves, and geopetal st...

Published: 01 June 2009
Figure 3. Photographs of calc-silicate xenoliths, sheeting, enclaves, and geopetal structures. (A) Fine-grained (pale gray) syenitic sheets with bulbous contacts with white, coarse-grained syenitic host on their east sides and subplanar contacts on their western sides. View to north-northwest
Image
Simplified schematic drawing of the difference in geopetal-fill crystal sizes as a consequence of differences in nucleation and growth rates. A) Crystal sizes of quartz formed during filling of void under initially high and subsequently decreasing temperatures. B) Crystal sizes of quartz formed during filling of void under isothermal conditions.

Simplified schematic drawing of the difference in geopetal-fill crystal siz...

Published: 01 March 2005
Figure 9 Simplified schematic drawing of the difference in geopetal-fill crystal sizes as a consequence of differences in nucleation and growth rates. A) Crystal sizes of quartz formed during filling of void under initially high and subsequently decreasing temperatures. B) Crystal sizes
Image
A) Rotated geopetal structures in foraminifera embedded in dark marl as indicated by white arrows; sample Cap 59. B) Accumulation of broken foraminifera (a) in an organic-rich matrix (gray marl); Cap 20. C) Condensed microlayer (&lt; 1 mm) composed of phosphatic particles (a), foraminifera (with rotated geopetal structure: b) and bone fragments (c); Cap 59. D) Siliceous agglutinated benthic foraminifera (a) preserved in a red marl; Cap 111. E) Condensed phosphatic horizon containing light-colored phosphatic nodules (a), bone fragments (b), "soft" sediment pebble (organic-rich mudstone = c), organic-rich matrix (d), and wood fragments (e); Cap 144A. F) Condensed phosphatic horizon; phosphatic matrix contains phosphatized foraminifera (a) and coated grains (b); Cap 140a. G) Foraminifera coated with phosphate (a); Cap 47. H) Multilayered phosphate-coated grain (a); Cap 101. I) Phosphate-coated grains coalesced into a multi-compound nodule. Individual coated grains (a) and foraminifera (b) are still recognizable; Cap 50. J) Concentration of phosphatic particles and nodules (a); Cap 128. K) a cohesive phosphatic level overlain by an organic-rich layer; b = benthic foraminifer; Cap 62. L) Large phosphatic nodule (a) in a dark and homogeneous marl; Cap 130. M) Superimposed phosphatic layers (a) in an organic-rich matrix; Cap 62. N) Phosphatic lenses increasingly densely packed toward the top, probably because of winnowing events of increasing strength; Cap. 62.

A) Rotated geopetal structures in foraminifera embedded in dark marl as in...

Published: 01 March 2002
Figure 4 A) Rotated geopetal structures in foraminifera embedded in dark marl as indicated by white arrows; sample Cap 59. B) Accumulation of broken foraminifera (a) in an organic-rich matrix (gray marl); Cap 20. C) Condensed microlayer (< 1 mm) composed of phosphatic particles
Image
A) Plate-like coral with geopetal peloidal micrite infilling the growth-framework porosity (arrow). Although the original coralline carbonate has been dissolved, the growth structure is visible because of micritization. B) Locally, the original microstructure of corals is preserved as relicts within neomorphic calcite.

A) Plate-like coral with geopetal peloidal micrite infilling the growth-fr...

Published: 01 May 2001
Figure 5 A) Plate-like coral with geopetal peloidal micrite infilling the growth-framework porosity (arrow). Although the original coralline carbonate has been dissolved, the growth structure is visible because of micritization. B) Locally, the original microstructure of corals is preserved
Image
Examples of the cement infilling ammonite body chambers with geopetal infill. (a) Plane‐polarized light micrograph illustrating the geopetal infill and cements within an ammonite body chamber. Note the majority of the primary porosity is infilled by a peloidal sediment (p), the presence of an early inclusion‐rich turbid calcite cement and a later, inclusion‐poor calcite cement (c). Scale bar 340 μm. (b) Cathodoluminescence micrograph showing the same field of view as (a). This micrograph illustrates that the blotchy and highly variable luminescence characteristics of the peloidal sediment, the presence of an early dull luminescing zone (arrowed 1) which is enclosed by a later bright luminescing zone (arrowed 2). Moreover, it also shows that the later inclusion‐poor calcite comprises an early bright luminescing calcite (arrowed 3), and later dull luminescing calcite (arrowed 4 and 5). Scale bar 340 μm.

Examples of the cement infilling ammonite body chambers with geopetal infil...

Published: 01 January 2000
Fig. 3. Examples of the cement infilling ammonite body chambers with geopetal infill. ( a ) Plane‐polarized light micrograph illustrating the geopetal infill and cements within an ammonite body chamber. Note the majority of the primary porosity is infilled by a peloidal sediment (p), the presence
Image
—Types of geopetal fabrics recognized in reef complexes.

—Types of geopetal fabrics recognized in reef complexes.

Published: 01 June 1980
FIG. 19 —Types of geopetal fabrics recognized in reef complexes.
Image
—Diagram illustrating use of geopetal fabrics as fossil spirit levels to distinguish depositional and postdepositional dip components.

—Diagram illustrating use of geopetal fabrics as fossil spirit levels to di...

Published: 01 June 1980
FIG. 20 —Diagram illustrating use of geopetal fabrics as fossil spirit levels to distinguish depositional and postdepositional dip components.
Image
—Histograms illustrating geopetal measurements used in determining postdepositional dip component in Sadler Limestone on west side of McWhae Ridge.

—Histograms illustrating geopetal measurements used in determining postdepo...

Published: 01 June 1980
FIG. 22 —Histograms illustrating geopetal measurements used in determining postdepositional dip component in Sadler Limestone on west side of McWhae Ridge.
Image
—Diagram illustrating geopetal fabrics present in Sadler Limestone on west side of McWhae Ridge (Fig. 11).

—Diagram illustrating geopetal fabrics present in Sadler Limestone on west ...

Published: 01 June 1980
FIG. 21 —Diagram illustrating geopetal fabrics present in Sadler Limestone on west side of McWhae Ridge ( Fig. 11 ).
Image
—Different specimen, same outcrop as Figure 8. Slope of dark geopetal fill implies left-to-right drift of depositing currents.

—Different specimen, same outcrop as Figure 8 . Slope of dark geopetal fil...

Published: 01 April 1973
FIG. 11. —Different specimen, same outcrop as Figure 8 . Slope of dark geopetal fill implies left-to-right drift of depositing currents.