Mississippian

@book{zeller1950stratigraphic2,
    author = "Zeller, E. J",
    title = "Stratigraphic significance of Mississippian endothyroid Foraminifera",
    year = "1950",
    publisher = "University of Kansas Paleontological Contributions, p. 1-23; Protozoa, article 4",
    note = "talkorigins\_source = {true}; raw\_reference = {Zeller, E. J., 1950, Stratigraphic significance of Mississippian endothyroid Foraminifera: University of Kansas Paleontological Contributions, p. 1-23; Protozoa, article 4.}"
}

The stratigraphic column in the Confusion Range extends from Ordovician(?) through Triassic. Mississippian and Pennsylvanian strata were studied in detail and one composite section was diagrammed. Slightly more than 6,000 feet of Devonian strata were recognized. They consist for the most part of massive, black limestone beds containing an Upper Devonian fauna. The massive limestone beds are overlain by shaly limestone beds that contain a Cyrtospirifer fauna. The Mississippian system is represented by only 260 feet of strata, assigned to the Midridge formation, that appear to be correlative with some part of the Mission Canyon formation of Montana. No rocks of Burlington, Keokuk, Meramec, and Chester ages were found in the area. The Pennsylvanian system consists of slightly more than 3,700 feet of sediments that contain an abundant, well preserved fauna of Morrow age. The Pennsylvanian sediments are cyclic and are interpreted to indicate gradual submergence of the area. Beds in the lower part of the Morrow sequence have heretofore been assigned to the Mississippian.

@article{ogden1951mississippian,
    author = "Ogden, Lawrence",
    title = "Mississippian and Pennsylvanian Stratigraphy, Confusion Range, West-Central Utah",
    year = "1951",
    journal = "AAPG Bulletin",
    abstract = "The stratigraphic column in the Confusion Range extends from Ordovician(?) through Triassic. Mississippian and Pennsylvanian strata were studied in detail and one composite section was diagrammed. Slightly more than 6,000 feet of Devonian strata were recognized. They consist for the most part of massive, black limestone beds containing an Upper Devonian fauna. The massive limestone beds are overlain by shaly limestone beds that contain a Cyrtospirifer fauna. The Mississippian system is represented by only 260 feet of strata, assigned to the Midridge formation, that appear to be correlative with some part of the Mission Canyon formation of Montana. No rocks of Burlington, Keokuk, Meramec, and Chester ages were found in the area. The Pennsylvanian system consists of slightly more than 3,700 feet of sediments that contain an abundant, well preserved fauna of Morrow age. The Pennsylvanian sediments are cyclic and are interpreted to indicate gradual submergence of the area. Beds in the lower part of the Morrow sequence have heretofore been assigned to the Mississippian.",
    url = "https://doi.org/10.1306/3d934145-16b1-11d7-8645000102c1865d",
    doi = "10.1306/3d934145-16b1-11d7-8645000102c1865d",
    number = "1",
    openalex = "W2049954327",
    pages = "62-82",
    volume = "35",
    references = "doi101130001676061948591027gotcrw20co2, doi101130001676061948591027kpscrw20co2, doi101130spe25p1, doi1013063d93345416b111d78645000102c1865d, doi103133b391, doi103133pp111, doi103133pp153, doi103133pp171, doi103133wsp277, doi105962bhltitle23478"
}

This paper is based on a detailed stratigraphic restudy of the lower part of the Madison group at the type section in Montana; and a section, measured bed by bed, of the Madison limestone near Logan, Utah, is compared with the type section. A new formation which underlies the Madison in northeastern Utah is described and compared with the Sappington sandstone which underlies the Madison at the type section. Both on a lithologic and faunal basis the Sappington and the new unit appear to be contemporaneous formations. The Sappington appears to be Kinderhookian since the typical Upper Devonian Cyrtospirifer fauna was not found above, or the Lower Mississippian Syringothyris fauna below, a thin black shale at the base of the Sappington. The Lodgepole limestone, lowermost formation of the Madison group, overlies the Sappington. It consists of a remarkable sequence of dark gray, hard, very fine-crystalline limestones rhythmically interbedded with softer light gray to yellowish gray, argillaceous limestone or shale. The fauna of the Lodgepole indicates that it too is entirely Kinderhookian. In northeastern Utah Devonian fossils were found at the top of a prominent limestone ledge the base of which was previously believed to mark the base of the Madison. This ledge is now assigned to the Jefferson formation of the Devonian. The new formation, made up of a series of shales, sandy shales, and nodular limestones, unconformably overlies the ledge now attributed to the Jefferson and carries the same Syringothyris fauna as the Sappington sandstone of Montana. The base of the Madison limestone is accordingly drawn at the base of 30 feet of brownish black fissile shale which overlies this new formation. Above this basal shale unit the Madison consists of dark gray, fine-crystalline limestone rhythmically interbedded with shaly limestone beds. The similarity of the lithology, especially the rhythmic nature of the bedding, combined with the faunal similarities, indicates that the Madison in this area is entirely Lodgepole in age. There are apparently no beds equivalent to upper Madison, that is, the Mission Canyon limestone of Montana, in the Utah section.

@article{holland1952stratigraphic,
    author = "Holland, F. D.",
    title = "Stratigraphic Details of Lower Mississippian Rocks of Northeastern Utah and Southwestern Montana",
    year = "1952",
    journal = "AAPG Bulletin",
    abstract = "This paper is based on a detailed stratigraphic restudy of the lower part of the Madison group at the type section in Montana; and a section, measured bed by bed, of the Madison limestone near Logan, Utah, is compared with the type section. A new formation which underlies the Madison in northeastern Utah is described and compared with the Sappington sandstone which underlies the Madison at the type section. Both on a lithologic and faunal basis the Sappington and the new unit appear to be contemporaneous formations. The Sappington appears to be Kinderhookian since the typical Upper Devonian Cyrtospirifer fauna was not found above, or the Lower Mississippian Syringothyris fauna below, a thin black shale at the base of the Sappington. The Lodgepole limestone, lowermost formation of the Madison group, overlies the Sappington. It consists of a remarkable sequence of dark gray, hard, very fine-crystalline limestones rhythmically interbedded with softer light gray to yellowish gray, argillaceous limestone or shale. The fauna of the Lodgepole indicates that it too is entirely Kinderhookian. In northeastern Utah Devonian fossils were found at the top of a prominent limestone ledge the base of which was previously believed to mark the base of the Madison. This ledge is now assigned to the Jefferson formation of the Devonian. The new formation, made up of a series of shales, sandy shales, and nodular limestones, unconformably overlies the ledge now attributed to the Jefferson and carries the same Syringothyris fauna as the Sappington sandstone of Montana. The base of the Madison limestone is accordingly drawn at the base of 30 feet of brownish black fissile shale which overlies this new formation. Above this basal shale unit the Madison consists of dark gray, fine-crystalline limestone rhythmically interbedded with shaly limestone beds. The similarity of the lithology, especially the rhythmic nature of the bedding, combined with the faunal similarities, indicates that the Madison in this area is entirely Lodgepole in age. There are apparently no beds equivalent to upper Madison, that is, the Mission Canyon limestone of Montana, in the Utah section.",
    url = "https://doi.org/10.1306/5ceadb8a-16bb-11d7-8645000102c1865d",
    doi = "10.1306/5ceadb8a-16bb-11d7-8645000102c1865d",
    number = "9",
    openalex = "W2030118156",
    pages = "1697-1734",
    volume = "36",
    references = "doi1011300016760619485991cotmfo20co2, doi101130001676061949601mfosnm20co2, doi101130gsab531729, doi101130gsab54591, doi101130spe14, doi1013063d93360816b111d78645000102c1865d, doi1013063d933a1016b111d78645000102c1865d, doi1013063d933ef016b111d78645000102c1865d, ogden1951mississippian, openalexw1509454543, openalexw1932910858, openalexw2955031006"
}

Some 400 cephalopods were recently collected from a shale zone in the Mississippian strata of the Confusion Range in central western Utah. This fauna includes representatives of the genera Mooreoceras, Bactrites, Goniatites, Lyro- goniatites, Neoglyphioceras, Girtyoceras?, Dimorphoceras, and Epicanites. Two new species, referable to Lyrogoniatites and Epicanites, are described and illustrated, along with representative specimens of the other genera. A brief discussion of the associated pelecypods is included. The containing beds are considered to be Mera- mec in age and to be the approximate equivalent of the cephalopod-bearing por- tions of the Heath formation of Montana, the White Pine shale of Nevada and California, the Helms and Barnett formations of Texas, the Caney shale of Okla- homa, and the upper Visean of Europe.

@article{openalexw2525893777,
    author = "Miller, Arthur K. and Youngquist, Walter Lewellyn and Nielsen, Merrill L.",
    title = "Mississippian cephalopods from western Utah",
    year = "1952",
    journal = "Journal of Paleontology",
    abstract = "Some 400 cephalopods were recently collected from a shale zone in the Mississippian strata of the Confusion Range in central western Utah. This fauna includes representatives of the genera Mooreoceras, Bactrites, Goniatites, Lyro- goniatites, Neoglyphioceras, Girtyoceras?, Dimorphoceras, and Epicanites. Two new species, referable to Lyrogoniatites and Epicanites, are described and illustrated, along with representative specimens of the other genera. A brief discussion of the associated pelecypods is included. The containing beds are considered to be Mera- mec in age and to be the approximate equivalent of the cephalopod-bearing por- tions of the Heath formation of Montana, the White Pine shale of Nevada and California, the Helms and Barnett formations of Texas, the Caney shale of Okla- homa, and the upper Visean of Europe.",
    openalex = "W2525893777",
    references = "ogden1951mississippian"
}

The value of smaller foraminifera in Upper Palaeozoic stratigraphy is enhanced greatly by the adoption of an integrated procedure of analysis, using assemblages from both the hard and the soft rocks of any one sequence. This partial fusion of the solid and thin-section analytical methods reveals the inadequacies of each when employed singly. Its combined character leads to much greater accuracy in palaeontological and stratigraphic studies, and, at the same time, indicates many of its own limitations. In the present paper, examples are drawn from the British Avonian Palaeotextulariidae to illustrate the combined method. The faunal analysis and stratigraphic application of Upper Palaeozoic smaller foraminifera

@article{doi1023071484248,
    author = "Cummings, Robert H.",
    title = "The Faunal Analysis and Stratigraphic Application of Upper Palaeozoic Smaller Foraminifera",
    year = "1958",
    journal = "Micropaleontology",
    abstract = "The value of smaller foraminifera in Upper Palaeozoic stratigraphy is enhanced greatly by the adoption of an integrated procedure of analysis, using assemblages from both the hard and the soft rocks of any one sequence. This partial fusion of the solid and thin-section analytical methods reveals the inadequacies of each when employed singly. Its combined character leads to much greater accuracy in palaeontological and stratigraphic studies, and, at the same time, indicates many of its own limitations. In the present paper, examples are drawn from the British Avonian Palaeotextulariidae to illustrate the combined method. The faunal analysis and stratigraphic application of Upper Palaeozoic smaller foraminifera",
    url = "https://doi.org/10.2307/1484248",
    doi = "10.2307/1484248",
    openalex = "W2314832324"
}

@article{openalexw2602597393,
    author = "Woodland, Roland Bert",
    title = "Stratigraphic significance of Mississippian endothyroid foraminifera in central Utah",
    year = "1958",
    journal = "Journal of Paleontology",
    url = "https://openalex.org/W2602597393",
    openalex = "W2602597393"
}

@article{woodland1958stratigraphic1,
    author = "Woodland, R. B",
    title = "Stratigraphic significance of Mississippian endothyroid Foraminifera in central Utah",
    year = "1958",
    journal = "Journal of Paleontology, v. 32, p. 791-814",
    note = "talkorigins\_source = {true}; raw\_reference = {Woodland, R. B., 1958, Stratigraphic significance of Mississippian endothyroid Foraminifera in central Utah: Journal of Paleontology, v. 32, p. 791-814.}"
}

ABSTRACT Work by the United States Geological Survey in the Confusion Range of west-central Utah during the past few years has resulted in the accumulation of considerable data regarding the stratigraphy of rocks ranging in age from Late Mississippian through Early Triassic. These rocks are here discussed as six formations, whose physical limits more or less coincide with the boundaries selected by earlier workers in the area, although considerable changes in stratigraphic nomenclature have been made. The Ely limestone of Late Mississippian, Early and Middle Pennsylvanian, and Permian age consists of 1,850–2,000 feet of alternating resistant thick-bedded limestone and slabby slope-forming limestone. The upper 100–350 feet of the formation contains an early Permian fauna and is generally more massive and less cherty than the remainder of the formation, which contains a fauna characteristic of the lower half of the Pennsylvanian and locally Late Mississippian. A hiatus representing Late Pennsylvanian time separates Middle Pennsylvanian and Permian faunas. The Arcturus formation, which conformably overlies the Ely limestone, consists of poorly indurated yellowish gray calcareous sandstone with thin, ledge-forming interbeds of dark gray to tan limestone and dolomite. The few fossils found in the Arcturus formation, and its stratigraphic position, suggest that the formation is early to middle Permian in age. The total thickness of the formation is uncertain, but a minimum thickness of 2,700 feet has been measured. The succeeding three formational units, the Kaibab limestone, the Plympton formation (new name), and the Gerster limestone, all of Permian age, have been included in the Park City group. The Kaibab limestone overlies the Arcturus formation and consists of 480 feet of somewhat cherty bioclastic limestone. The lithologic character of the Kaibab is in sharp contrast to the succeeding unit which is here named the Plympton formation and is predominantly dolomite and chert. The Plympton formation is 690 feet thick and contains phosphatic beds believed to be lithologic correlatives with parts of the Park City formation of northwestern Utah. The overlying Gerster limestone consists of 1,100 feet of very fossiliferous cherty bioclastic limestone and argillaceous limestone. The Gerster limestone is the youngest Permian unit in the Confusion Range. Like the Kaibab, it is differentiated from the Plympton formation by its high limestone content and lack of dolomite. The contact between the Plympton and the Gerster hmestone is conformable throughout the area. The Kaibab limestone, the Plympton formation, and the Gerster limestone are believed to be correlative with units within the Park City and related formations of nearby areas in northern and northwestern Utah and northeastern Nevada. In areas south of the Confusion Range, the younger Permian units, the Plympton formation, and the Gerster limestone, are absent and only the Kaibab limestone is present in the Grand Canyon area. The Thaynes formation of late Early Triassic age consists of thick beds of predominantly greenish gray calcareous clay shale interbedded with thin beds of gray to chocolate brown limestone, and is more than 1,900 feet thick in the Confusion Range. It is unconformably overlain by Tertiary and Quaternary strata, and no younger Mesozoic rocks crop out in the area. The contact of the Thaynes formation with the underlying Gerster limestone appears conformable; however, faunal evidence indicates a considerable hiatus between the two formations.

@article{doi1013060bda5ea616bd11d78645000102c1865d,
    author = "Hose, Richard Kenneth and Repenning, Charles Albert",
    title = "Stratigraphy of Pennsylvanian, Permian, and Lower Triassic Rocks of Confusion Range, West-Central Utah",
    year = "1959",
    journal = "AAPG Bulletin",
    abstract = "ABSTRACT Work by the United States Geological Survey in the Confusion Range of west-central Utah during the past few years has resulted in the accumulation of considerable data regarding the stratigraphy of rocks ranging in age from Late Mississippian through Early Triassic. These rocks are here discussed as six formations, whose physical limits more or less coincide with the boundaries selected by earlier workers in the area, although considerable changes in stratigraphic nomenclature have been made. The Ely limestone of Late Mississippian, Early and Middle Pennsylvanian, and Permian age consists of 1,850–2,000 feet of alternating resistant thick-bedded limestone and slabby slope-forming limestone. The upper 100–350 feet of the formation contains an early Permian fauna and is generally more massive and less cherty than the remainder of the formation, which contains a fauna characteristic of the lower half of the Pennsylvanian and locally Late Mississippian. A hiatus representing Late Pennsylvanian time separates Middle Pennsylvanian and Permian faunas. The Arcturus formation, which conformably overlies the Ely limestone, consists of poorly indurated yellowish gray calcareous sandstone with thin, ledge-forming interbeds of dark gray to tan limestone and dolomite. The few fossils found in the Arcturus formation, and its stratigraphic position, suggest that the formation is early to middle Permian in age. The total thickness of the formation is uncertain, but a minimum thickness of 2,700 feet has been measured. The succeeding three formational units, the Kaibab limestone, the Plympton formation (new name), and the Gerster limestone, all of Permian age, have been included in the Park City group. The Kaibab limestone overlies the Arcturus formation and consists of 480 feet of somewhat cherty bioclastic limestone. The lithologic character of the Kaibab is in sharp contrast to the succeeding unit which is here named the Plympton formation and is predominantly dolomite and chert. The Plympton formation is 690 feet thick and contains phosphatic beds believed to be lithologic correlatives with parts of the Park City formation of northwestern Utah. The overlying Gerster limestone consists of 1,100 feet of very fossiliferous cherty bioclastic limestone and argillaceous limestone. The Gerster limestone is the youngest Permian unit in the Confusion Range. Like the Kaibab, it is differentiated from the Plympton formation by its high limestone content and lack of dolomite. The contact between the Plympton and the Gerster hmestone is conformable throughout the area. The Kaibab limestone, the Plympton formation, and the Gerster limestone are believed to be correlative with units within the Park City and related formations of nearby areas in northern and northwestern Utah and northeastern Nevada. In areas south of the Confusion Range, the younger Permian units, the Plympton formation, and the Gerster limestone, are absent and only the Kaibab limestone is present in the Grand Canyon area. The Thaynes formation of late Early Triassic age consists of thick beds of predominantly greenish gray calcareous clay shale interbedded with thin beds of gray to chocolate brown limestone, and is more than 1,900 feet thick in the Confusion Range. It is unconformably overlain by Tertiary and Quaternary strata, and no younger Mesozoic rocks crop out in the area. The contact of the Thaynes formation with the underlying Gerster limestone appears conformable; however, faunal evidence indicates a considerable hiatus between the two formations.",
    url = "https://doi.org/10.1306/0bda5ea6-16bd-11d7-8645000102c1865d",
    doi = "10.1306/0bda5ea6-16bd-11d7-8645000102c1865d",
    openalex = "W2116818054",
    references = "ogden1951mississippian"
}

ABSTRACT The Brazer dolomite in its type area consists of about 850 feet of dolomite with a few beds of quartz sandstone and limestone near the top. Although poorly fossiliferous, the lower two-thirds of the formation has yielded a fauna of Early Mississippian age that suggests correlation with the Mission Canyon limestone of the type Madison group. The upper third of the formation contains a meager fauna of uncertain affinities, interpreted as Late Mississippian in age. Inasmuch as the Brazer can not be recognized on a lithologic or faunal basis outside the type area, it is recommended that the name be restricted to the Mississippian dolomite sequence in the Crawford Mountains. New nomenclature should be devised for the Upper Mississippian limestone-sandstone facies, previously called Brazer, in the northern Cordilleran region.

@article{doi1013060bda5f4b16bd11d78645000102c1865d,
    author = "Sando, J. T. Dutro W. J. and Dutro, J. T. and Gere, W. C.",
    title = "Brazer Dolomite (Mississippian), Randolph Quadrangle, Northeast Utah",
    year = "1959",
    journal = "AAPG Bulletin",
    abstract = "ABSTRACT The Brazer dolomite in its type area consists of about 850 feet of dolomite with a few beds of quartz sandstone and limestone near the top. Although poorly fossiliferous, the lower two-thirds of the formation has yielded a fauna of Early Mississippian age that suggests correlation with the Mission Canyon limestone of the type Madison group. The upper third of the formation contains a meager fauna of uncertain affinities, interpreted as Late Mississippian in age. Inasmuch as the Brazer can not be recognized on a lithologic or faunal basis outside the type area, it is recommended that the name be restricted to the Mississippian dolomite sequence in the Crawford Mountains. New nomenclature should be devised for the Upper Mississippian limestone-sandstone facies, previously called Brazer, in the northern Cordilleran region.",
    url = "https://doi.org/10.1306/0bda5f4b-16bd-11d7-8645000102c1865d",
    doi = "10.1306/0bda5f4b-16bd-11d7-8645000102c1865d",
    openalex = "W2152453125",
    references = "holland1952stratigraphic"
}

@article{geroch1959stratigraphic,
    author = "Geroch, Stanislaw",
    title = "Stratigraphic significance of arenaceous Foraminifera in the Carpathian Flysch",
    year = "1959",
    journal = "Paläontologische Zeitschrift",
    url = "https://doi.org/10.1007/bf02988984",
    doi = "10.1007/bf02988984",
    number = "1-2",
    openalex = "W2008942944",
    pages = "113-122",
    volume = "33",
    references = "openalexw2336749383, openalexw2605783363"
}

X 5 1 -5associated anhydrites.Turner Valley formation -370' -crinoidal limestones in the lower part to dolomitic limestones and dolomites in the upper.Shunda formation -190* -lithographic limestones, dolomites.Pekisko formation -3401 -crinoidal and oolitic limestones.Banff formation -510' -argillaceous cherty limestones to crinoidal limestones.From both a mega-and microfaunal standpoint the Moose Mount ain section is not fossiliferous.Although the crinoidal beds of the upper Banff formation were extensively thin-sectioned, no Foraminifera were found.A significant microfauna was noted only in the middle and upper Peki sko formation and lowermost Turner Valley formation.Of 62

@book{doi105962bhltitle153830,
    author = "McKay, Mary Winifred.",
    title = "Mississippian foraminifera of the southern Canadian Rockies, Alberta",
    year = "1961",
    booktitle = "University of Alberta eBooks",
    abstract = "X 5 1 -5associated anhydrites.Turner Valley formation -370' -crinoidal limestones in the lower part to dolomitic limestones and dolomites in the upper.Shunda formation -190* -lithographic limestones, dolomites.Pekisko formation -3401 -crinoidal and oolitic limestones.Banff formation -510' -argillaceous cherty limestones to crinoidal limestones.From both a mega-and microfaunal standpoint the Moose Mount ain section is not fossiliferous.Although the crinoidal beds of the upper Banff formation were extensively thin-sectioned, no Foraminifera were found.A significant microfauna was noted only in the middle and upper Peki sko formation and lowermost Turner Valley formation.Of 62",
    url = "https://doi.org/10.5962/bhl.title.153830",
    doi = "10.5962/bhl.title.153830",
    openalex = "W2898101054",
    references = "doi101098rsta19820032, doi101144gsljgs1948104010411, doi101144pygs2274, doi1013060bda5c3616bd11d78645000102c1865d, doi101306sv17349, doi1023071484248, openalexw2360519909, openalexw2602597393, openalexw2605631456, openalexw2612389506"
}

@article{brooks1962late,
    author = "Brooks, James E.",
    title = "Late Devonian--Early Mississippian Correlations Central Wasatch Mountains, Utah: ABSTRACT",
    year = "1962",
    journal = "AAPG Bulletin",
    url = "https://doi.org/10.1306/bc743785-16be-11d7-8645000102c1865d",
    doi = "10.1306/bc743785-16be-11d7-8645000102c1865d",
    openalex = "W2090749442",
    volume = "46"
}

The Late Osage to Meramec Arroyo Penasco Formation, 10-130 ft thick, rests on a peneplained surface of Precambrian rocks and is overlain unconformably by sediments of Pennsylvanian age. The Arroyo Penasco Formation crops out in the San Pedro, Nacimiento, Jemez, Sandia, Manzanita, Manzano, and Sangre de Cristo Mountains of north-central New Mexico. The basal unit, 2-60 ft thick, is transgressive and is composed of quartz conglomerate, sandstone, and thin shale. Three incomplete carbonate depositional cycles were recognized. The lowest, Cycle 1, consists of dolomite, dedolomite, and coarse-grained poikilotopic calcite with corroded dolomite rhombs. These rocks contain gray nodular chert with a microfauna of Late Osage age: Endothyra spinosa Chernysheva, E. skippae n. sp., and Septabrunsiina parakrainica Skipp, Holcomb, and Gutschick. The sediments of the earliest cycle show initial deposition as shallow-marine lime mudstone followed by stromatolitic intertidal to supratidal carbonate rocks. Cycle 2 is shallow-marine to intertidal echinoderm wackestone to lime mudstone and dolomite containing a sparse fauna of Endothyra aff. E. spinosa Chernysheva, Endothyra aff. E. irregularis (Zeller), E. irregularis (Zeller), and E. spiroides Zeller of Early Meramec age. Cycle 3 is shallow-marine wackestone to arenaceous oolitic to ooid-echinoderm packstone ending as subtidal lime and mudstone to intertidal dolomite. The ooid facies contains a rich microfauna of Early to Middle Meramec age: Endothyra prodigiosa Armstrong, E. macra Zeller, E. irregulari Endothyra, E. (Zeller) aff. E. omphalota Rauser-Cernoussova and Reitlinger, and Tournayella sp. Late Mississippian and Early Pennsylvanian uplift and erosion resulted in extensive erosion and removal of the Arroyo Penasco Formation. A solution limestone collapse breccia, 5-30 ft thick, rests on smooth surface of stromatolite dedolomite in the Sangre de Cristo Mountains. The breccia resulted from movement of meteoric ground waters in Late Mississippian or Early Pennsylvanian time. These dissolved a 5-30 ft thick gypsum bed and caused subsequent collapse of adjacent overlying Lower Meramec carbonate rocks. Solution activity was extensive, and sinkholes developed. This study, hopefully, will provide a regional understanding of the biostratigraphic and facies relationship of the Mississippian strata in north-central New Mexico with the Leadville Limestone of the San Juan Basin and the San Juan Mountains of Colorado and the Mississippian carbonate rocks of south-central and southern New Mexico. The known outcrops of Mississippian strata in north-central New Mexico were examined and measured, and lithologic and micropaleontologic samples were collected at five-ft intervals. The Mississippian and Devonian rocks of the San Juan Mountains of southwestern Colorado were examined and two sections carefully measured and studied: the classical section at Rockwood Quarry above Durango and the section at Davis' Creek in the Piedra River Canyon. The Kelly and Caloso Formations in the southern Ladron Mountains were also sampled and studied in thin sections. All shale samples were treated with sodium bicarbonate, washed and screened, and then picked under a binocular microscope for microfossils. A number of carbonate-rock suites were dissolved in formic acid, screened, and separated in heavy liquids for conodonts. The lithologic samples were cut for petrographic thinsections that were made for carbonate and foraminifera studies.

@book{doi1058799m20,
    author = "Armstrong, Augustus K.",
    title = "Biostratigraphy and carbonate facies of the Mississippian Arroyo Penasco Formation, north-central New Mexico",
    year = "1967",
    abstract = "The Late Osage to Meramec Arroyo Penasco Formation, 10-130 ft thick, rests on a peneplained surface of Precambrian rocks and is overlain unconformably by sediments of Pennsylvanian age. The Arroyo Penasco Formation crops out in the San Pedro, Nacimiento, Jemez, Sandia, Manzanita, Manzano, and Sangre de Cristo Mountains of north-central New Mexico. The basal unit, 2-60 ft thick, is transgressive and is composed of quartz conglomerate, sandstone, and thin shale. Three incomplete carbonate depositional cycles were recognized. The lowest, Cycle 1, consists of dolomite, dedolomite, and coarse-grained poikilotopic calcite with corroded dolomite rhombs. These rocks contain gray nodular chert with a microfauna of Late Osage age: Endothyra spinosa Chernysheva, E. skippae n. sp., and Septabrunsiina parakrainica Skipp, Holcomb, and Gutschick. The sediments of the earliest cycle show initial deposition as shallow-marine lime mudstone followed by stromatolitic intertidal to supratidal carbonate rocks. Cycle 2 is shallow-marine to intertidal echinoderm wackestone to lime mudstone and dolomite containing a sparse fauna of Endothyra aff. E. spinosa Chernysheva, Endothyra aff. E. irregularis (Zeller), E. irregularis (Zeller), and E. spiroides Zeller of Early Meramec age. Cycle 3 is shallow-marine wackestone to arenaceous oolitic to ooid-echinoderm packstone ending as subtidal lime and mudstone to intertidal dolomite. The ooid facies contains a rich microfauna of Early to Middle Meramec age: Endothyra prodigiosa Armstrong, E. macra Zeller, E. irregulari Endothyra, E. (Zeller) aff. E. omphalota Rauser-Cernoussova and Reitlinger, and Tournayella sp. Late Mississippian and Early Pennsylvanian uplift and erosion resulted in extensive erosion and removal of the Arroyo Penasco Formation. A solution limestone collapse breccia, 5-30 ft thick, rests on smooth surface of stromatolite dedolomite in the Sangre de Cristo Mountains. The breccia resulted from movement of meteoric ground waters in Late Mississippian or Early Pennsylvanian time. These dissolved a 5-30 ft thick gypsum bed and caused subsequent collapse of adjacent overlying Lower Meramec carbonate rocks. Solution activity was extensive, and sinkholes developed. This study, hopefully, will provide a regional understanding of the biostratigraphic and facies relationship of the Mississippian strata in north-central New Mexico with the Leadville Limestone of the San Juan Basin and the San Juan Mountains of Colorado and the Mississippian carbonate rocks of south-central and southern New Mexico. The known outcrops of Mississippian strata in north-central New Mexico were examined and measured, and lithologic and micropaleontologic samples were collected at five-ft intervals. The Mississippian and Devonian rocks of the San Juan Mountains of southwestern Colorado were examined and two sections carefully measured and studied: the classical section at Rockwood Quarry above Durango and the section at Davis' Creek in the Piedra River Canyon. The Kelly and Caloso Formations in the southern Ladron Mountains were also sampled and studied in thin sections. All shale samples were treated with sodium bicarbonate, washed and screened, and then picked under a binocular microscope for microfossils. A number of carbonate-rock suites were dissolved in formic acid, screened, and separated in heavy liquids for conodonts. The lithologic samples were cut for petrographic thinsections that were made for carbonate and foraminifera studies.",
    url = "https://doi.org/10.58799/m-20",
    doi = "10.58799/m-20",
    openalex = "W4323764994",
    references = "doi101002gj3350020103, doi101016s0016787861800217, doi10113000167606196677843tsbp20co2, doi10130674d708942b2111d78648000102c1865d, doi10130674d711952b2111d78648000102c1865d, doi10130674d7131b2b2111d78648000102c1865d, doi1023072406301, doi1058799b79, doi1058799m8, openalexw2761886851"
}

Part I: The Joyita uplift is a documented key to the central New Mexico late Virgilian and early Wolfcampian episode of erosion and accompanying deposition of clastic strata. Detailed studies of the lithologies and fusulinid faunas of the Pennsylvanian and Early Permian rocks confirm this uplift and the related unconformity. The present-day Joyita Hills (Los Canoncitos) is a complex Cenozoic horst on the east side of the Rio Grande graben in north-central Socorro County, New Mexico. Previous reports postulated a nearby uplift during late Desmoinesian, Missourian, and Virgilian time coexistence with the Penasco or southern Unconpahgre landmass. Recently (1963), Missourian fusulinids were identified from upper Pennsylvanian limestones in the Joyita Hills. Early Wolfcampian Bursum-facies arkosic limestone-conglomerates, derived from Pennsylvanian limestones and Precambrian granite gneiss of southern Joyita Hills area, unconformably truncate southwestward, in order, Missourian, Desmoinesian, Atokan, and Precambrian rocks. In southern Joyita Hills, Bursum strata abut against remnant hills of Precambrian granite gneiss. These hills were buried by basal Abo red beds which, adjacent to the hills, gradationally overlie Bursum purplish-green shales and limestones. Joyita Hills area, lying east of the Lucero Basin and southwest of the Estancia Basin, was a submarine platform with small, low islands during Atokan and Desmoinesian time, as attested by black Atokan shales and Desmoinesian arkosic limestone-pebble conglomerate. The thinness of remnant upper Pennsylvanian strata is believed due mainly to erosion during early Wolfcampian time, not owing to erosion during late Desmoinesian, Missourian, or early Virgilian times. As the early Wolfcampian Bursum facies, bearing a Schwagerina and Tricites fauna, is unconformably on Virgilian beds in many parts of central New Mexico, the Joyita uplift is a documented key to this late Virgilian and early Wolfcampian episode of erosion and of accompanying deposition of clastic strata. Structural features of Pennsylvanian age in north-central and south-central New Mexico appear to have been aligned roughly north-south. Major sediment traps in north-central New Mexico during Pennsylvanian time were the Rowe-Mora Basin(or Taos trough of Sutherland), in central New Mexico the Estancia Basin and Lucero Basin, and in south-central New Mexico the Orogrande Basin and San Mateo Basin. Source areas for these sediments were the Uncompahgre, Penasco, Pedernal, and Zuni uplifts. The Joyita uplift is on the east flank of the Lucero Basin and on the southwest margin of the Estancia Basin; its present-day elevated expression dates from late Tertiary time, but pre-Mesozoic strata are relatively thin in the Joyita Hills. Part II: Fusulinids occur in great abundance throughout the interval of Pennsylvanian sediments in the Joyita Hills. A new genus Parafusulinella is described with two new species, P. propria from the Joyita Hills, and P. mexicana from the Boca Grande Mountains of northwestern Mexico. Other new species described from the Joyita Hills include Plectofusulina rotunda, P. coelocamara, P. fusiformis, Beedeina joyitaensis, Wedekindellina elongata, W. alveolata, Triticites riograndensis, and T. liosepta. The stratigraphic occurrence of the fusulinids, their biozones and paleoecological significance have been discussed in Part I of this study. Additional discussion concerning stratigraphy, faunal assemblages, taxonomy, systematic descriptions, and phylogeny follows. All specimens and types are filed in the Texaco Inc. paleontological collections.

@book{doi1058799m23,
    author = "Kottlowski, Frank Ε. and Stewart, Wendell J.",
    title = "Part I: The Wolfcampian Joyita uplift in central New Mexico: Part II: Fusulinids of the Joyita Hills, Socorro County, central New Mexico",
    year = "1970",
    abstract = "Part I: The Joyita uplift is a documented key to the central New Mexico late Virgilian and early Wolfcampian episode of erosion and accompanying deposition of clastic strata. Detailed studies of the lithologies and fusulinid faunas of the Pennsylvanian and Early Permian rocks confirm this uplift and the related unconformity. The present-day Joyita Hills (Los Canoncitos) is a complex Cenozoic horst on the east side of the Rio Grande graben in north-central Socorro County, New Mexico. Previous reports postulated a nearby uplift during late Desmoinesian, Missourian, and Virgilian time coexistence with the Penasco or southern Unconpahgre landmass. Recently (1963), Missourian fusulinids were identified from upper Pennsylvanian limestones in the Joyita Hills. Early Wolfcampian Bursum-facies arkosic limestone-conglomerates, derived from Pennsylvanian limestones and Precambrian granite gneiss of southern Joyita Hills area, unconformably truncate southwestward, in order, Missourian, Desmoinesian, Atokan, and Precambrian rocks. In southern Joyita Hills, Bursum strata abut against remnant hills of Precambrian granite gneiss. These hills were buried by basal Abo red beds which, adjacent to the hills, gradationally overlie Bursum purplish-green shales and limestones. Joyita Hills area, lying east of the Lucero Basin and southwest of the Estancia Basin, was a submarine platform with small, low islands during Atokan and Desmoinesian time, as attested by black Atokan shales and Desmoinesian arkosic limestone-pebble conglomerate. The thinness of remnant upper Pennsylvanian strata is believed due mainly to erosion during early Wolfcampian time, not owing to erosion during late Desmoinesian, Missourian, or early Virgilian times. As the early Wolfcampian Bursum facies, bearing a Schwagerina and Tricites fauna, is unconformably on Virgilian beds in many parts of central New Mexico, the Joyita uplift is a documented key to this late Virgilian and early Wolfcampian episode of erosion and of accompanying deposition of clastic strata. Structural features of Pennsylvanian age in north-central and south-central New Mexico appear to have been aligned roughly north-south. Major sediment traps in north-central New Mexico during Pennsylvanian time were the Rowe-Mora Basin(or Taos trough of Sutherland), in central New Mexico the Estancia Basin and Lucero Basin, and in south-central New Mexico the Orogrande Basin and San Mateo Basin. Source areas for these sediments were the Uncompahgre, Penasco, Pedernal, and Zuni uplifts. The Joyita uplift is on the east flank of the Lucero Basin and on the southwest margin of the Estancia Basin; its present-day elevated expression dates from late Tertiary time, but pre-Mesozoic strata are relatively thin in the Joyita Hills. Part II: Fusulinids occur in great abundance throughout the interval of Pennsylvanian sediments in the Joyita Hills. A new genus Parafusulinella is described with two new species, P. propria from the Joyita Hills, and P. mexicana from the Boca Grande Mountains of northwestern Mexico. Other new species described from the Joyita Hills include Plectofusulina rotunda, P. coelocamara, P. fusiformis, Beedeina joyitaensis, Wedekindellina elongata, W. alveolata, Triticites riograndensis, and T. liosepta. The stratigraphic occurrence of the fusulinids, their biozones and paleoecological significance have been discussed in Part I of this study. Additional discussion concerning stratigraphy, faunal assemblages, taxonomy, systematic descriptions, and phylogeny follows. All specimens and types are filed in the Texaco Inc. paleontological collections.",
    url = "https://doi.org/10.58799/m-23",
    doi = "10.58799/m-23",
    openalex = "W4323793919"
}

ABSTRACT Carboniferous rocks above the Milligen Formation in the central Lost River Range of south-central Idaho range in age from Late Mississippian (middle Meramecian or middle Viséan) through Pennsylvanian (Atokan or Westphalian), as determined by small calcareous foraminifers, corals, and brachiopods. The lower part of the post-Milligen sequence, composed largely of limestone, is Mississippian and is divided into four formations first described by Huh in the Lemhi and Lost River Ranges. These rocks are overlain by an unnamed Pennsylvanian sandstone unit which, in turn, is overlain by a thick sequence of unnamed Pennsylvanian limestone. The composite section in the Lost River Range has a minimum exposed thickness of 7,000 ft. Two partial sections in the Hawley Mountains are designated reference sections for the four formations of Mississippian age In the Lost River Range—the Middle Canyon Formation at the base, the Scott Peak Formation, the South Creek Formation, and the Surrett Canyon Formation at the top. Foraminiferal Zones 13(?) through 21 are recognized in the Carboniferous rocks. Zone 19, the Homoceras ammonoid time equivalent, is described herein for the first time from North America. Representatives of megafaunal Zones Pre-E through Post-K are also recognized in the Mississippian and the directly overlying rocks of the Carboniferous sequence. Microfaunas and megafaunas indicate that the Meramec-Chester boundary is near the middle of the Scott Peak Formation, that the Viséan-Namurian boundary is near the base of the Surrett Canyon Formation, and that the Mississippian-Pennsylvanian boundary is about at the base of the unnamed sandstone unit. Carbonate lithologies and associated faunas and microfaunas indicate deposition in a marine environment in which there was a general change from quiet water having locally restricted circulation during Middle Canyon Formation deposition to turbulent water that was freely circulating during deposition of the upper strata. Sand in the basal Pennsylvanian rocks may indicate a distant orogenic pulse very near the Mississippian-Pennsylvanian time boundary.

@article{doi1013065d25cdd116c111d78645000102c1865d,
    author = "Mamet, Bernard and Skipp, Betty and Sando, William J. and Mapel, W.J.",
    title = "Biostratigraphy of Upper Mississippian and Associated Carboniferous Rocks in South-Central Idaho",
    year = "1971",
    journal = "AAPG Bulletin",
    abstract = "ABSTRACT Carboniferous rocks above the Milligen Formation in the central Lost River Range of south-central Idaho range in age from Late Mississippian (middle Meramecian or middle Viséan) through Pennsylvanian (Atokan or Westphalian), as determined by small calcareous foraminifers, corals, and brachiopods. The lower part of the post-Milligen sequence, composed largely of limestone, is Mississippian and is divided into four formations first described by Huh in the Lemhi and Lost River Ranges. These rocks are overlain by an unnamed Pennsylvanian sandstone unit which, in turn, is overlain by a thick sequence of unnamed Pennsylvanian limestone. The composite section in the Lost River Range has a minimum exposed thickness of 7,000 ft. Two partial sections in the Hawley Mountains are designated reference sections for the four formations of Mississippian age In the Lost River Range—the Middle Canyon Formation at the base, the Scott Peak Formation, the South Creek Formation, and the Surrett Canyon Formation at the top. Foraminiferal Zones 13(?) through 21 are recognized in the Carboniferous rocks. Zone 19, the Homoceras ammonoid time equivalent, is described herein for the first time from North America. Representatives of megafaunal Zones Pre-E through Post-K are also recognized in the Mississippian and the directly overlying rocks of the Carboniferous sequence. Microfaunas and megafaunas indicate that the Meramec-Chester boundary is near the middle of the Scott Peak Formation, that the Viséan-Namurian boundary is near the base of the Surrett Canyon Formation, and that the Mississippian-Pennsylvanian boundary is about at the base of the unnamed sandstone unit. Carbonate lithologies and associated faunas and microfaunas indicate deposition in a marine environment in which there was a general change from quiet water having locally restricted circulation during Middle Canyon Formation deposition to turbulent water that was freely circulating during deposition of the upper strata. Sand in the basal Pennsylvanian rocks may indicate a distant orogenic pulse very near the Mississippian-Pennsylvanian time boundary.",
    url = "https://doi.org/10.1306/5d25cdd1-16c1-11d7-8645000102c1865d",
    doi = "10.1306/5d25cdd1-16c1-11d7-8645000102c1865d",
    openalex = "W2128753134",
    references = "doi1013060bda635316bd11d78645000102c1865d"
}

This study was planned to examine, sample, and evaluate biostratigraphically important Mississippian sections across the northwestern quadrant of Utah

@article{doi103133ofr76200,
    author = "Gutschick, Raymond C.",
    title = "Preliminary reconnaissance study of Lower and lower Upper Mississippian strata across northwestern Utah",
    year = "1976",
    journal = "Antarctica A Keystone in a Changing World",
    abstract = "This study was planned to examine, sample, and evaluate biostratigraphically important Mississippian sections across the northwestern quadrant of Utah",
    url = "https://doi.org/10.3133/ofr76200",
    doi = "10.3133/ofr76200",
    openalex = "W103106802",
    references = "doi103133pp842, ogden1951mississippian"
}

Approximately 1,400 m (meters) (4,600 ft or feet) of interbedded carbonate rocks, sandstone, siltstone, and mudstone of latest Mississippian to Early Permian age are assigned to the Arco Hills, Bluebird Mountain, and Snaky Canyon Formations in eastcentral Idaho north of the Snake River Plain.The Snaky Canyon Formation (largely Permian and Pennsylvanian, locally including latest Mississippian) is divided into three members, which are, in ascending order, Bloom, Gallagher Peak Sandstone, and Juniper Gulch.The new formations have been recognized, from west to east, in the southern Pioneer and White Knob Mountains, the southern Lemhi and Lost River Ranges, and the Beaverhead Mountains.The carbonate-bank sequence is overridden on the west by the Copper Basin allochthon and extends no farther east than the Medicine Lodge thrust.An arbitrary northern limit for the terminology is proposed at about latitude 44°30'.The Arco Hills Formation (uppermost Mississippian) is underlain by the Surrett Canyon Formation of Late Mississippian age.The Bluebird Mountain Formation (uppermost Mississippian) is underlain by the White Knob Limestone in the central White Knob Mountains and by the Surrett Canyon Formation in the southern White Knob and Pioneer Mountains.From the Lost River Range east to the Blue Dome area of the southern Beaverhead Mountains, the Bluebird Mountain Formation is underlain by the Arco Hills Formation.In the remainder of the southern Beaverhead Mountains it is underlain by the Big Snowy Formation.The Snaky Canyon Formation (Lower Permian to uppermost Mississippian) overlies the Bluebird Mountain Formation and is overlain by the Phosphoria Formation in the southern Lemhi Range and Beaverhead Mountains, and by unnamed Permian beds in the White Knob Mountains.A remnant of the Triassic Dinwoody Formation is preserved above the Phosphoria Formation in the southern Beaverhead Mountains.Sandstones in the Bluebird Mountain and Snaky Canyon Formations generally thin westward toward the Copper Basin allochthon and, thus, are not reworked flysch deposits.They are composed of craton-derived detritus which spread as far west as the

@misc{doi103133b1486,
    author = "Skipp, Betty and Hoggan, R.D. and Schleicher, David and Douglass, Raymond C.",
    title = "Upper Paleozoic carbonate bank in east-central Idaho: Snaky Canyon, Bluebird Mountain, and Arco Hills Formations, and their paleotectonic significance",
    year = "1979",
    abstract = "Approximately 1,400 m (meters) (4,600 ft or feet) of interbedded carbonate rocks, sandstone, siltstone, and mudstone of latest Mississippian to Early Permian age are assigned to the Arco Hills, Bluebird Mountain, and Snaky Canyon Formations in eastcentral Idaho north of the Snake River Plain.The Snaky Canyon Formation (largely Permian and Pennsylvanian, locally including latest Mississippian) is divided into three members, which are, in ascending order, Bloom, Gallagher Peak Sandstone, and Juniper Gulch.The new formations have been recognized, from west to east, in the southern Pioneer and White Knob Mountains, the southern Lemhi and Lost River Ranges, and the Beaverhead Mountains.The carbonate-bank sequence is overridden on the west by the Copper Basin allochthon and extends no farther east than the Medicine Lodge thrust.An arbitrary northern limit for the terminology is proposed at about latitude 44°30'.The Arco Hills Formation (uppermost Mississippian) is underlain by the Surrett Canyon Formation of Late Mississippian age.The Bluebird Mountain Formation (uppermost Mississippian) is underlain by the White Knob Limestone in the central White Knob Mountains and by the Surrett Canyon Formation in the southern White Knob and Pioneer Mountains.From the Lost River Range east to the Blue Dome area of the southern Beaverhead Mountains, the Bluebird Mountain Formation is underlain by the Arco Hills Formation.In the remainder of the southern Beaverhead Mountains it is underlain by the Big Snowy Formation.The Snaky Canyon Formation (Lower Permian to uppermost Mississippian) overlies the Bluebird Mountain Formation and is overlain by the Phosphoria Formation in the southern Lemhi Range and Beaverhead Mountains, and by unnamed Permian beds in the White Knob Mountains.A remnant of the Triassic Dinwoody Formation is preserved above the Phosphoria Formation in the southern Beaverhead Mountains.Sandstones in the Bluebird Mountain and Snaky Canyon Formations generally thin westward toward the Copper Basin allochthon and, thus, are not reworked flysch deposits.They are composed of craton-derived detritus which spread as far west as the",
    url = "https://doi.org/10.3133/b1486",
    doi = "10.3133/b1486",
    openalex = "W1542399946",
    references = "doi1013060bda635316bd11d78645000102c1865d"
}

Abstract Analysis of biostratigraphic relations in central North America permits recognition of a generalized, widely applicable depositional model for late Early Mississippian (=Tournaisian 3 and early Osagean) strata. Depositional strike paralleled the low, but subaerial, southwest-northeast trending Transcontinental Arch. Four depositional magnafacies (Carbonate Shelf, Starved, Novaculitic and Clastic) are discernible and the Carbonate Shelf Magnafacies can be further subdivided into Inner Shelf, Main Shelf and Shelf Margin Depofacies. The areal distribution of the four magnafacies is similar to such depositional facies in the European Lower Carboniferous, where the carbonate shelf deposits are called ‘Kohlenkalk’ or ‘Carboniferous Limestone’ and the other three have been referred to collectively as the ‘Culm’ Facies.

@article{openalexw1524370185,
    author = "Lane, H. Richard and Keyser, Timothy",
    title = "Paleogeography of the Late Early Mississippian (Tournaisian 3) in the Central and Southwestern United States",
    year = "1980",
    abstract = "Abstract Analysis of biostratigraphic relations in central North America permits recognition of a generalized, widely applicable depositional model for late Early Mississippian (=Tournaisian 3 and early Osagean) strata. Depositional strike paralleled the low, but subaerial, southwest-northeast trending Transcontinental Arch. Four depositional magnafacies (Carbonate Shelf, Starved, Novaculitic and Clastic) are discernible and the Carbonate Shelf Magnafacies can be further subdivided into Inner Shelf, Main Shelf and Shelf Margin Depofacies. The areal distribution of the four magnafacies is similar to such depositional facies in the European Lower Carboniferous, where the carbonate shelf deposits are called ‘Kohlenkalk’ or ‘Carboniferous Limestone’ and the other three have been referred to collectively as the ‘Culm’ Facies.",
    openalex = "W1524370185"
}

@misc{crossref1981distribution,
    title = "Distribution and stratigraphic significance of foraminifera and algae in well cores from Madison Group (Mississippian), Williston Basin, Montana",
    year = "1981",
    url = "https://doi.org/10.3133/b1529f",
    doi = "10.3133/b1529f",
    openalex = "W1549791392",
    references = "doi1013060bda5ca516bd11d78645000102c1865d, doi1013063d93360816b111d78645000102c1865d, doi103133pp526b, doi103133pp554b, doi103133pp613e, doi103133pp842, openalexw2257577903, openalexw2262253166, openalexw2264008598"
}

Fusulinid Foraminifera from Pennsylvanian strata in the Manzano Mountains, central New Mexico, indicate that the Sandia Formation (Atokan) lies in the zone of Fusulinella, and that the Los Moyos Limestone (Desmoinesian) lies mostly in the zone of Beedeina. Two assemblage subzones recognized in the Sandia Formation are those of Fusulinella devexa and F. whitensis. Four assemblage subzones recognized in the Los Moyos Limestone are those of Beedeina insolita, B. novamexicana, B. rockymontana, and B. sulphurensis. The presence of Eowaeringella in the uppermost beds of the Los Moyos Limestone indicates that the beds are of earliest Missourian age.

@article{doi103133pp1446,
    author = "Myers, Donald A.",
    title = "Stratigraphic distribution of fusulinid foraminifera from the Manzano Mountains, New Mexico",
    year = "1988",
    journal = "USGS professional paper",
    abstract = "Fusulinid Foraminifera from Pennsylvanian strata in the Manzano Mountains, central New Mexico, indicate that the Sandia Formation (Atokan) lies in the zone of Fusulinella, and that the Los Moyos Limestone (Desmoinesian) lies mostly in the zone of Beedeina. Two assemblage subzones recognized in the Sandia Formation are those of Fusulinella devexa and F. whitensis. Four assemblage subzones recognized in the Los Moyos Limestone are those of Beedeina insolita, B. novamexicana, B. rockymontana, and B. sulphurensis. The presence of Eowaeringella in the uppermost beds of the Los Moyos Limestone indicates that the beds are of earliest Missourian age.",
    url = "https://doi.org/10.3133/pp1446",
    doi = "10.3133/pp1446",
    openalex = "W1582624758",
    references = "doi1058799m20"
}

The Lower Mississippian Mission Canyon Formation and stratigraphic equivalents in Montana and Idaho were deposited on a progradational carbonate ramp that developed on the foreland side of the Antler foredeep. Shallow subtidal and peritidal lithofacies were deposited in ramp-interior settings across most of Montana. The ramp to basin transition in westernmost Montana was a relatively narrow belt of stacked skeletal grainstone banks. Farther west, skeletal grainstone banks prograded over and interfingered with outer ramp/slope cherty limestones. In east-central Idaho, coeval lower slope and basinal strata consisted of silty to argillaceous, spicular limestones, spiculites, and spicular calcareous siltstones/fine-grained sandstones.

@incollection{doi101306m57579c13,
    author = "Reid, S. K. and Dorobek, S. L.",
    title = "Sequence Stratigraphy and Evolution of a Progradational, Foreland Carbonate Ramp, Lower Mississippian Mission Canyon Formation and Stratigraphic Equivalents, Montana and Idaho",
    year = "1993",
    booktitle = "American Association of Petroleum Geologists eBooks",
    abstract = "The Lower Mississippian Mission Canyon Formation and stratigraphic equivalents in Montana and Idaho were deposited on a progradational carbonate ramp that developed on the foreland side of the Antler foredeep. Shallow subtidal and peritidal lithofacies were deposited in ramp-interior settings across most of Montana. The ramp to basin transition in westernmost Montana was a relatively narrow belt of stacked skeletal grainstone banks. Farther west, skeletal grainstone banks prograded over and interfingered with outer ramp/slope cherty limestones. In east-central Idaho, coeval lower slope and basinal strata consisted of silty to argillaceous, spicular limestones, spiculites, and spicular calcareous siltstones/fine-grained sandstones.",
    url = "https://doi.org/10.1306/m57579c13",
    doi = "10.1306/m57579c13",
    openalex = "W1568786066",
    references = "doi103133pp842"
}

Endothyroid foraminifers are common in most marine Pennsylvanian units in the Appalachian Basin. The genera Planoendothyra Reitlinger, 1959, and Endothyranella Galloway and Harlton, 1930, are the dominant taxa. Scarce Endothyra Phillips, 1846, are restricted below the Desmoinesian. The greatest change in stratigraphic distribution of taxa occurs at the Atokan-Desmoinesian boundary. Sixteen taxa are recognized. Five new species are proposed, including Planoendothyra orbiculata, P.? associata, Endothyranella kentuckyensis, E. inflata, and E. intermissa. Most taxa are assigned previously described American species using a cf. designation. Description and thin section illustration provide a basis for nomenclatural acceptance of these taxa.

@article{hoare1998pennsylvanian,
    author = "Hoare, R. D. and Sturgeon, M. T.",
    title = "Pennsylvanian endothyroid foraminifera from the Appalachian Basin",
    year = "1998",
    journal = "Journal of Paleontology",
    abstract = "Endothyroid foraminifers are common in most marine Pennsylvanian units in the Appalachian Basin. The genera Planoendothyra Reitlinger, 1959, and Endothyranella Galloway and Harlton, 1930, are the dominant taxa. Scarce Endothyra Phillips, 1846, are restricted below the Desmoinesian. The greatest change in stratigraphic distribution of taxa occurs at the Atokan-Desmoinesian boundary. Sixteen taxa are recognized. Five new species are proposed, including Planoendothyra orbiculata, P.? associata, Endothyranella kentuckyensis, E. inflata, and E. intermissa. Most taxa are assigned previously described American species using a cf. designation. Description and thin section illustration provide a basis for nomenclatural acceptance of these taxa.",
    url = "https://doi.org/10.1017/s002233600002415x",
    doi = "10.1017/s002233600002415x",
    number = "3",
    openalex = "W2485514913",
    pages = "405-418",
    volume = "72",
    references = "doi1010079781489957603, doi101017s0022336000036003, doi101144pygs2274, doi10130674d720682b2111d78648000102c1865d, doi102113gsjfr144282, doi1023071485456, openalexw2625570274, openalexw2735133573, openalexw592310489, openalexw650457216"
}

ABSTRACT This study describes the sedimentology and stratigraphy of the Devonian–Mississippian Sappington Formation in exceptional outcrop exposures in southwestern Montana. The goal was to assess the extent to which these outcrops could be used to define stratigraphic heterogeneity of time-equivalent Bakken Formation reservoir and source rocks of the Williston Basin. Facies analysis of the Sappington Formation shows three depositional sequences deposited along a storm- and wave-influenced coastline. The first sequence encompasses the lower Sappington shale, dominated by organic-rich mudstones that represent an anoxic to dysoxic lower-shelf environment. The second sequence is marked by a basal transgressive surface and initial siltstone deposition. These siltstones are abruptly overlain by basinward-dipping, low-angle clinoforms (<1°) that represent a storm- and wave-influenced shoreface. Facies distributions along clinoforms change along depositional dip over approximately 17 km (∼11 mi) from proximal to distal across the study area. The best reservoir facies are present in the upper foresets of these clinoforms. The upper shale of the Sappington Formation forms the lowest part of the third depositional sequence that continues into the overlying Lodgepole Limestone. The outcrop-based stratigraphy of the Sappington Formation provides insights into the scale of stratigraphic heterogeneity that is likely to be present in the time-equivalent Bakken Formation over the length of a typical approximately 3-km-long (∼2-mi-long) horizontal well. Geosteering horizontal wells in the Bakken along bedding surfaces, that is, along gently dipping clinoforms, is likely to cause variations in rock properties from the toe to heel of a horizontal well.

@article{doi1013060627171614817020,
    author = "Phelps, Anna S. and Hofmann, Michaël and Hart, Bruce S.",
    title = "Facies and stratigraphic architecture of the Upper Devonian–Lower Mississippian Sappington Formation, southwestern Montana: A potential outcrop analog for the Bakken Formation",
    year = "2018",
    journal = "AAPG Bulletin",
    abstract = "ABSTRACT This study describes the sedimentology and stratigraphy of the Devonian–Mississippian Sappington Formation in exceptional outcrop exposures in southwestern Montana. The goal was to assess the extent to which these outcrops could be used to define stratigraphic heterogeneity of time-equivalent Bakken Formation reservoir and source rocks of the Williston Basin. Facies analysis of the Sappington Formation shows three depositional sequences deposited along a storm- and wave-influenced coastline. The first sequence encompasses the lower Sappington shale, dominated by organic-rich mudstones that represent an anoxic to dysoxic lower-shelf environment. The second sequence is marked by a basal transgressive surface and initial siltstone deposition. These siltstones are abruptly overlain by basinward-dipping, low-angle clinoforms (\<1°) that represent a storm- and wave-influenced shoreface. Facies distributions along clinoforms change along depositional dip over approximately 17 km (∼11 mi) from proximal to distal across the study area. The best reservoir facies are present in the upper foresets of these clinoforms. The upper shale of the Sappington Formation forms the lowest part of the third depositional sequence that continues into the overlying Lodgepole Limestone. The outcrop-based stratigraphy of the Sappington Formation provides insights into the scale of stratigraphic heterogeneity that is likely to be present in the time-equivalent Bakken Formation over the length of a typical approximately 3-km-long (∼2-mi-long) horizontal well. Geosteering horizontal wells in the Bakken along bedding surfaces, that is, along gently dipping clinoforms, is likely to cause variations in rock properties from the toe to heel of a horizontal well.",
    url = "https://doi.org/10.1306/0627171614817020",
    doi = "10.1306/0627171614817020",
    openalex = "W2799677474",
    references = "holland1952stratigraphic"
}

Abstract In the Big Snowy Mountains of central Montana, USA, late Visean to Bashkirian strata preserve a nearly complete, but poorly documented, paleotropical stratigraphic succession that straddles the range of current estimates of the onset of the Late Paleozoic Ice Age (LPIA). Sedimentologic and stratigraphic investigation of the Otter (late Visean to Serpukhovian) and Heath (Serpukhovian) formations, with secondary focus on the overlying Tyler (late Serpukhovian to Bashkirian) and Alaska Bench (Bashkirian) formations, facilitated an appraisal of paleotropical environmental change preserved in this succession. Three facies associations reminiscent of environments currently forming in Shark Bay, Australia, were identified in the Otter Formation: shallow semi-restricted littoral platform, intertidal platform, and supratidal plain. Five facies associations broadly comparable to modern environments present in the Sunda Shelf and southern coast of the Persian Gulf were identified in the Heath Formation: offshore outer ramp, mid- to outer ramp, inner ramp, coastal plain, and sabkha. Facies associations preserved in the Heath Formation are here explained in the context of a protected, homoclinal carbonate ramp situated in a partially silled epicontinental embayment. A shift from low-magnitude relative sea-level oscillations preserved in the Otter Formation to a cyclothemic stratigraphic pattern entailing ≥ 6 fourth-order, high-frequency and high-magnitude relative sea-level fluctuations in the Heath Formation is here interpreted to record the main eustatic signal of the LPIA in central Montana. Current published biostratigraphic constraints for the observed stratigraphy estimate the main eustatic signal of the LPIA to have occurred approximately between 331 (base Serpukhovian) and 327 Ma in central Montana. A distinct upward transition from coal and paleosol-bearing depositional sequences in the lower Heath to evaporite and limestone-bearing depositional sequences in the upper Heath preserves a broad humid to arid paleoclimate shift during deposition of this unit, which influenced hydrographic circulation patterns and the resultant distribution of anoxic environments in the Big Snowy Trough during this time interval. Improved depositional and sequence stratigraphic models of the Heath Formation proposed in this study permit new insight into the theoretical distribution of, and water depth necessary to preserve, black, organic-rich claystone and shale in partially silled intracratonic basins, in addition to new temporal constraints on LPIA onset in paleotropical western Laurentia.

@article{doi102110jsr201944,
    author = "Ahern, Justin P. and Fielding, Christopher R.",
    title = "Onset of the Late Paleozoic Glacioeustatic Signal: A Stratigraphic Record from the Paleotropical, Oil-Shale-Bearing Big Snowy Trough of Central Montana, U.S.A.",
    year = "2019",
    journal = "Journal of Sedimentary Research",
    abstract = "Abstract In the Big Snowy Mountains of central Montana, USA, late Visean to Bashkirian strata preserve a nearly complete, but poorly documented, paleotropical stratigraphic succession that straddles the range of current estimates of the onset of the Late Paleozoic Ice Age (LPIA). Sedimentologic and stratigraphic investigation of the Otter (late Visean to Serpukhovian) and Heath (Serpukhovian) formations, with secondary focus on the overlying Tyler (late Serpukhovian to Bashkirian) and Alaska Bench (Bashkirian) formations, facilitated an appraisal of paleotropical environmental change preserved in this succession. Three facies associations reminiscent of environments currently forming in Shark Bay, Australia, were identified in the Otter Formation: shallow semi-restricted littoral platform, intertidal platform, and supratidal plain. Five facies associations broadly comparable to modern environments present in the Sunda Shelf and southern coast of the Persian Gulf were identified in the Heath Formation: offshore outer ramp, mid- to outer ramp, inner ramp, coastal plain, and sabkha. Facies associations preserved in the Heath Formation are here explained in the context of a protected, homoclinal carbonate ramp situated in a partially silled epicontinental embayment. A shift from low-magnitude relative sea-level oscillations preserved in the Otter Formation to a cyclothemic stratigraphic pattern entailing ≥ 6 fourth-order, high-frequency and high-magnitude relative sea-level fluctuations in the Heath Formation is here interpreted to record the main eustatic signal of the LPIA in central Montana. Current published biostratigraphic constraints for the observed stratigraphy estimate the main eustatic signal of the LPIA to have occurred approximately between 331 (base Serpukhovian) and 327 Ma in central Montana. A distinct upward transition from coal and paleosol-bearing depositional sequences in the lower Heath to evaporite and limestone-bearing depositional sequences in the upper Heath preserves a broad humid to arid paleoclimate shift during deposition of this unit, which influenced hydrographic circulation patterns and the resultant distribution of anoxic environments in the Big Snowy Trough during this time interval. Improved depositional and sequence stratigraphic models of the Heath Formation proposed in this study permit new insight into the theoretical distribution of, and water depth necessary to preserve, black, organic-rich claystone and shale in partially silled intracratonic basins, in addition to new temporal constraints on LPIA onset in paleotropical western Laurentia.",
    url = "https://doi.org/10.2110/jsr.2019.44",
    doi = "10.2110/jsr.2019.44",
    openalex = "W2970366391",
    references = "doi1013060bda5ca516bd11d78645000102c1865d, doi103133pp554b, openalexw2257577903"
}

• This study presents foraminifers from the Mississippian Arroyo Peñasco Formation and basal Log Springs Formation, and the lower Pennsylvanian Osha Canyon Formation of north-central New Mexico, USA. • Foraminifers of the Arroyo Peñasco Formation (Espiritu Santo Member) indicate a Tournaisian age (MFZ 1–8). • Reworked limestone clasts of the basal Log Springs Formation contain foraminifers of late early Viséan age. • The Osha Canyon Formation contains a small foraminiferal assemblage indicating Morrowan age. In the Sierra Nacimiento-San Pedro Mountains-Jemez Mountains of north-central New Mexico (USA), the thin succession of Mississippian sediments is termed the Arroyo Peñasco Formation, overlain by the Log Springs Formation. The Arroyo Peñasco Formation is subdivided into Del Padre Member composed of siliciclastic sediments and the overlying Espiritu Santo Member composed of carbonate sediments. Foraminifers of the Espiritu Santo Member at Lion Spring in the northern San Pedro Mountains indicate a Tournaisian age. The lower Tournaisian (= Hastarian = biozones MFZ1-4 of Poty et al., 2006 [Geological Magazine 143, 829-857]) is locally characterized by Septaglomospiranella ex gr. primaeva, Septabrunsiina minuta and Tournayella sp. The upper Tournaisian (= Ivorian = biozones MFZ5-9 of Poty et al., 2006) is characterized by Spinoendothya, Inflatoendothyra and Tuberendothyra. In the Sierra Nacimiento-San Pedro Mountains-Jemez Mountains, the sediments of the Arroyo Peñasco Group are unconformably overlain by nonmarine redbeds of the Log Springs Formation (Serpukhovian/upper Chesterian). Some of the carbonate clasts of the basal conglomerate of the Log Springs Formation at Lion Spring contain late early Viséan (biozone MFZ11B of Poty et al., 2006) foraminifers and algae, including Koninckopora and Paraarchaediscus. These carbonate clasts are reworked from the underlying Arroyo Peñasco Formation (Espiritu Santo Member). In north-central New Mexico, a transgression during the Early Pennsylvanian (Morrowan) caused deposition of the shallow marine sediments of the Osha Canyon Formation. The Morrowan age of the Osha Canyon Formation is based on Nigrispiroides nov. gen., Iriclinella, Globivalvulina, and Millerella.

@article{doi101016jgeobios202411009,
    author = "Krainer, Karl and Lucas, Spencer G. and Vachard, Daniel",
    title = "Mississippian-Lower Pennsylvanian foraminifers from the Sierra Nacimiento and San Pedro Mountains, North-Central New Mexico, USA",
    year = "2025",
    journal = "Geobios",
    abstract = "• This study presents foraminifers from the Mississippian Arroyo Peñasco Formation and basal Log Springs Formation, and the lower Pennsylvanian Osha Canyon Formation of north-central New Mexico, USA. • Foraminifers of the Arroyo Peñasco Formation (Espiritu Santo Member) indicate a Tournaisian age (MFZ 1–8). • Reworked limestone clasts of the basal Log Springs Formation contain foraminifers of late early Viséan age. • The Osha Canyon Formation contains a small foraminiferal assemblage indicating Morrowan age. In the Sierra Nacimiento-San Pedro Mountains-Jemez Mountains of north-central New Mexico (USA), the thin succession of Mississippian sediments is termed the Arroyo Peñasco Formation, overlain by the Log Springs Formation. The Arroyo Peñasco Formation is subdivided into Del Padre Member composed of siliciclastic sediments and the overlying Espiritu Santo Member composed of carbonate sediments. Foraminifers of the Espiritu Santo Member at Lion Spring in the northern San Pedro Mountains indicate a Tournaisian age. The lower Tournaisian (= Hastarian = biozones MFZ1-4 of Poty et al., 2006 [Geological Magazine 143, 829-857]) is locally characterized by Septaglomospiranella ex gr. primaeva, Septabrunsiina minuta and Tournayella sp. The upper Tournaisian (= Ivorian = biozones MFZ5-9 of Poty et al., 2006) is characterized by Spinoendothya, Inflatoendothyra and Tuberendothyra. In the Sierra Nacimiento-San Pedro Mountains-Jemez Mountains, the sediments of the Arroyo Peñasco Group are unconformably overlain by nonmarine redbeds of the Log Springs Formation (Serpukhovian/upper Chesterian). Some of the carbonate clasts of the basal conglomerate of the Log Springs Formation at Lion Spring contain late early Viséan (biozone MFZ11B of Poty et al., 2006) foraminifers and algae, including Koninckopora and Paraarchaediscus. These carbonate clasts are reworked from the underlying Arroyo Peñasco Formation (Espiritu Santo Member). In north-central New Mexico, a transgression during the Early Pennsylvanian (Morrowan) caused deposition of the shallow marine sediments of the Osha Canyon Formation. The Morrowan age of the Osha Canyon Formation is based on Nigrispiroides nov. gen., Iriclinella, Globivalvulina, and Millerella.",
    url = "https://doi.org/10.1016/j.geobios.2024.11.009",
    doi = "10.1016/j.geobios.2024.11.009",
    openalex = "W4410616138",
    references = "doi101144sp512202042"
}