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Rattlesnake Canyon (maybe Petrolia Fm, but disputed): Protocaptorhinus, Aspidosaurus sp. (MCZ 1477), ''Orodus? corrugatus'',

upper Admiral Fm = Petrolia Fm

Mount Barry (IVf) is also Petrolia Fm

Vale Formation
The Vale Formation is a geological formation in north-central Texas, a component of the Texas red beds preserving sediments and fossils from the Early Permian Leonardian series. It occupies the middle part of the Clear Fork Group, above the Arroyo Formation and below the Choza Formation. Some sources consider the Vale Formation to be merely an informal subunit of the Clear Fork Formation, thus renaming it to the Middle Clear Fork Formation.

Geology
The Vale Formation is named after a former post office in the vicinity of Ballinger in Runnels County. At its broadest conception, the Vale Formation is a unit of primarily terrestrial sediments up to 160 m thick, stretching from the Texas-Oklahoma border at Wilbarger County, as far south as Runnels County. The base of the Vale Formation is marked by either a limestone bed (the Standpipe Limestone, south of Abilene), or in some northern areas, a sharp unconformity. Likewise, its contact with the Choza Formation is marked by the base of the Bullwagon Dolomite, which is most well-exposed south of Haskell, or by evaporite beds in northern exposures such as Knox County.

Limestone is rare in the fully terrestrial northern red beds, complicating the distinction between the three formations of the Clear Fork Group. To resolve this problem, some geologists, like Nelson et al. (2013), consider the northern part of the Clear Fork Group to be a single formation divided into three informal subunits. In the northern area, major sandstone beds are the most useful stratigraphic markers for distinguishing these informal subunits. The Middle Clear Fork Formation extends from the base of the Brushy Creek Sandstone to the base of the Rt. 1919 Sandstone. Another major sandstone bed, the Cedar Top Sandstone, occurs between these two levels.

As with much of the Texas red beds, the dominant sediments (around 80% by volume) are fine-grained red floodplain deposits such as mudstones, clays, shales, siltstones, and paleosols. Localized beds and lenses of sandstone and conglomerate recorded active meandering river channels, abandoned channels (such as oxbow lakes), and crevasse splays. The conglomerates of the Vale Formation occur in two distinct forms, either large light-colored fragments or (particularly in the northern area) dark brown pebbles derived from the surrounding clay. Light even-bedded clay (pond deposits) may occasionally be found.

Though quite fossiliferous, the fossils of the Vale Formation have not been studied as long as older parts of the Texas red beds, some of which have been prospected since the 1870s. Geologists of the University of Texas discovered the first fossils from the Vale Formation in the 1930s, at the Sid McAdams locality in Taylor County. Since 1946, many more finds were recovered from Knox, Baylor, and Foard counties under the direction of University of Chicago paleontologist Everett C. Olson, who described the northern Vale fossil fauna in detail over the course of the 1950s. Other notable sites include the Stamford locality in Haskell County (discovered by Dalquest and Maymay in 1963), the Blackwood locality in Taylor County (discovered by David Berman in 1970), and the Mud Hill locality (described by Bryan Gee et al. in 2018), also in Taylor County. Over 60 small fossil sites are scattered south of the Clear Fork of the Brazos River.

Reptiles
The largest true reptile known from the Vale Formation is an indeterminate moradisaurine captorhinid represented by an enormous tooth plate, at least 11.6 cm in length. This tooth plate was so large it was originally considered to be from an unnamed species of edaphosaurid, which would have made it the youngest known member of that family. As a moradisaurine fossil, it corresponds to a skull around 35 cm long, larger than Labidosaurikos meachami but smaller than Moradisaurus grandis.

Amphibians
An indeterminate hapsidopareiid microsaur is known from the Mud Hill locality. It is potentially one of the youngest known microsaurs, apart from a few rhynchonkids known from Choza-equivalent strata near Norman, Oklahoma.

Invertebrates
A few invertebrate fossils are known from the Sid McAdams locality. These include freshwater bivalves (?Palaenodonta) and a single well-preserved pygocephalomorph crustacean, Mamayocaris jespeni, a species which is abundant in Permian sediments of South Dakota.

Plants
Plant fossils of the middle Clear Fork are most well-preserved in fine-grained abandoned river channel deposits. Some abandoned channel sites are dominated by walchian conifers, Taeniopteris, and "comioid" peltasperms (Auritifolia). Others have a high proportion of woody gigantopterids (Evolsonia), Taeniopteris, and marattialean tree ferns. Tree ferns were probably most specialized for swampy areas alongside permanent water, while conifers occupied dry uplands. Peltasperms and gigantopterids were accustomed to intermediate conditions: well-drained soils with a high water table. A diverse array of insect damage is reported from leaf fossils, with particular preference towards Auritifolia and Taniopteris.

Treatise H citations
Whole Part Template (Cite book, note: no ISBN, since it varies between volumes):

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Extinctions
Other extinctions: Botomian, Dresbachian, Franconian, Trempealeauan, Caradoc?, Ireviken/Llandovery, Mulde/Wenlock, Pridoli?, Visean?, Scythian (Induan?, Smithian-Spathian?), Carnian?, Norian?, Aptian,

Lockatong Facies
Van Houter (1964 http://www.kgs.ku.edu/Publications/Bulletins/169/VanHouten/index.html), Smoot (1991 https://www.sciencedirect.com/science/article/abs/pii/003101829190055V)

Smoot & Olsen (1988- https://www.ldeo.columbia.edu/~polsen/nbcp/smoot_olsen_88_sm.pdf), Smoot & Olsen (1994), Smoot (2010), Olsen & Kent (1996)

Van Houten (1969-https://books.google.com/books?hl=en&lr=&id=so9MkARBrnAC&oi=fnd&pg=PA5#v=onepage&q&f=false)

TPS (1985-https://pubs.usgs.gov/circ/1985/0946/report.pdf#page=24)

Smoot et al (1985-https://pubs.geoscienceworld.org/aapgbull/article-abstract/69/9/1448/564270)

Van Houten 1969 suggested the Stockton/Lockatong/Passaic Formations correspond to specific time periods, while Smoot et al. (1985) and Turner-Peterson & Smoot (1985) suggested they were time-transgressive due to Gilbert-like deltaic sediments being present in both the Stockton and Lockatong formations.

Tumble Falls Member
A2 (black/grey hard argillite) followed by "Double Red" (red to black to red argillite) of McLaughlin 1944. Also discussed in Willard et al 1959. Informally named by Olsen 1986, formalized by Olsen et al 1996. Early in the section is the beginning of magnetozone E13n.1n. Nursery no. 1/Tutusville no. 1 core overlap. Some particularly thick, fine black shales. Type section at west slope of PA route 32 opposite the Delaware River from Tumble Falls, NJ. 218.51-218.11 Ma (Kent et al 2017 APTS)

Microbial spherules (https://link.springer.com/article/10.1007/s12549-015-0207-y).

Sedimentary structures and ichnotaxa: https://books.google.com/books?hl=en&lr=&id=n7mCDwAAQBAJ&oi=fnd&pg=PP1#v=onepage&q&f=false

McLaughlin 1944-Penn stratigraphy north of Point Pleasant: https://www.jstor.org/stable/44109261?seq=1#metadata_info_tab_contents

1945-Penn stratigraphy near Point Pleasant (no Tumble Fall outcrops): https://www.jstor.org/stable/44109298?seq=1#metadata_info_tab_contents

1946-New Jersey side stratigraphy: https://www.jstor.org/stable/44109327?seq=1#metadata_info_tab_contents

Willard et al 1959: https://archive.org/details/geologymineralre00penn/page/76/mode/2up

Olsen 1986: https://science.sciencemag.org/content/234/4778/842

Olsen et al 1996: https://pubs.geoscienceworld.org/gsa/gsabulletin/article-abstract/108/1/40/183081

supp. data: https://www.geosociety.org/datarepository/1996/9601.pdf

Smith Corner Member
Also Smith's or Smiths Corner. A1 (black/grey hard argillite) and "Smith's Corner Red Member" (thin band of red argillite) of McLaughlin 1944. Massive mudstone instead of black shale. Found in the Nursery core. Type section at west side of PA route 32 north of Point Pleasant, PA. Exposed at several places along Tohickon Creek, including a stream at the village of Smiths Corner, PA. 218.92-218.51 Ma (Kent et al 2017 APTS). Youngest Lockatong conchostracans: Wannerestheria pennsylvanica, no Howellisaura? ovata. This zone is also found in the basal Gettysburg Formation and has been considered Late Tuvalian by some (though criticized). Upper half of magnetozone E12r.

Kozur Weems 2010: https://sp.lyellcollection.org/content/334/1/315

Husing et al 2011: https://www.sciencedirect.com/science/article/abs/pii/S0012821X10007648

Olsen Kent Whiteside: https://www.cambridge.org/core/journals/earth-and-environmental-science-transactions-of-royal-society-of-edinburgh/article/implications-of-the-newark-supergroupbased-astrochronology-and-geomagnetic-polarity-time-scale-newarkapts-for-the-tempo-and-mode-of-the-early-diversification-of-the-dinosauria/FED0F73A12B28F7EA1696940D927C123

Prahls Island Member
"Triple Red" and the undifferentiated underlying black argillite of McLaughlin 1944. Massive mudstone instead of black shale. Type section at "Old Busik Quarry" at a Creek along the east side of NJ Route 29, south of Tumble Falls and near the southern part of Prahls Island. Also exposed near Locktown and Kingwood, NJ. Found in the Nursery core. Lower half of magnetozone E12r. Old Solite Quarry (o) of Cow Branch Formation equivalent to the lower half of Prahls Island Member based on magnetostratigraphy (E12r at Newark = D4r at Cow Branch). 218.92-219.32 Ma.

Kent Olsen 1997: https://www.ldeo.columbia.edu/~polsen/nbcp/kent.olsen.97.pdf

Selden et al 1999: http://www.paulselden.net/uploads/7/5/3/2/7532217/joaaraneomorphs.pdf

Smoot Olsen 1994 (differences between massive mudstone and black shale facies, etc.): https://pubs.geoscienceworld.org/books/book/1176/chapter/10575445/Climatic-Cycles-as-Sedimentary-Controls-of-Rift

Tohickon Member
"First Big Red" and the undifferentiated underlying black argillite of McLaughlin 1944. Type section at a creek on the east side of NJ Route 29, north of Byram. 219.32-219.73 Ma. E12n, upper extent of E11r. Found in the Nursery Core, the extensive Byram outcrop, and the Haines and Kibblehouse Quarry.

Smoot 2010 (more facies stuff): https://www.state.nj.us/dep/njgs/enviroed/oldpubs/bulletin77.pdf

Withjack et al 2012 (rift basin development): https://sp.lyellcollection.org/content/369/1/301

Skunk Hollow Member
"First Thin Red" and the upper extent of the underlying black argillite of McLaughlin 1944. Unusually thick black shales. Type section at Haines and Kibblehouse Quarry along Skunk Hollow Road in Hilltown township, PA. Also found at the Byram outcrop and Nursery Core. E11r. 219.73-220.13 Ma. Skunk Hollow Fish Bed.

Figure 50 in Non-Marine Boundary events Olsen

Byram Member
Type section at the NJ Route 29 outcrop north of Byram. Nursery and Princeton Cores, E11r, 220.13-220.54 Ma.

Silesauridae

 * Ankylothecodont dentition
 * Short, subtriangular dentition (not Lewisuchus)
 * Mesiodistally expanded tooth crowns? (not Lewisuchus)
 * Pointed front tip of Dentary (not Lewisuchus)
 * Toothless front tip of dentary (not Lewisuchus)
 * Narrow ventral process of the squamosal?
 * ICAs enter braincase ventrally? (not Lewisuchus)
 * Hypoglossal nerve exits anteroposteriorly aligned
 * Rugose anterolateral edges of the supraoccipital
 * Cervical centra 3-5 longer than middorsal
 * Sacral ribs shared between vertebrae? (not Lewisuchus) NO
 * Humeral head continuous with deltopectoral crest?
 * Rugosities on preacetabular and postacetabular processes of ilium
 * Straight ventral margin of ilium (not Kwanasaurus)
 * Thin, drooping "saddle-shaped" iliac blade (not Lewisuchus, Asilisaurus, or Lutungutali)
 * Femur longer than tibia? (not Lewisuchus)
 * Straight medial articular facet of femur (not Lewisuchus)
 * Groove on the femoral head?
 * Notch under femoral head
 * Hoof-like pedal unguals?

Like most early avemetatarsalians, the hip and hindlimbs of silesaurids are among the most informative parts of the skeleton. The ilium (upper blade of the hip) has a closed acetabulum, a "primitive" feature unlike the open acetabulum of dinosaurs. In almost all silesaurids, the acetabulum is positioned far back on the ilium, leading to its lower edge being represented primarily by the straight ischiadic peduncle. Dinosaurs (with the apparent exception of Saturnalia) have a concave lower edge due to the open acetabulum, and the only silesaurid with this advanced condition is possibly Kwanasaurus. More basal dinosauromorphs and other archosaurs have a primarily convex and wedge-shaped lower edge due to the pubic and ischiac peduncles having equal contribution to the lower edge.

The femoral head is offset from the rest of the shaft through an abrupt obtuse notch, rather than a continuous concave rim present in other dinosauromorphs. In most silesaurids, the femoral head is roughly triangular in cross section, connecting to the hip through a short flat surface. The most basal silesaurids, Lewisuchus and Asilisaurus, retain the more convex connection possessed by other archosaurs. All silesaurids apart from Lewisuchus have a straight groove on the top of the femoral head. Also in non-Lewisuchus silesaurids, the lower portion of the femur has a characteristic deep groove (seemingly the popliteal fossa) running up more than 1/4 of its rear edge.

Skull
The tooth-bearing maxilla bone of the snout was 16.5 centimeters (6.5 inches) in length and had 14 teeth. Although the front part of the tooth row was slightly upturned, most of it was straight and completely horizontal. There is a smoothly curved transition between the front edge of the maxilla and the upward-branching ascending process, which lies in front of the antorbital fenestra. These traits are generally in contrast to derived erythrosuchids like Erythrosuchus and Garjainia, which have a concave tooth row and an abrupt transition between the main body and ascending process of the maxilla. The rear edge of the ascending process has a slightly thickened area which curves downwards before diminishing, a trait also seen in Garjainia. Like many other basal archosauriforms, but in contrast to most erythrosuchids, the antorbital fenestra is not surrounded by a lowered basin of bone (known as an antorbital fossa). The teeth are ankylothecodont, meaning that they are fused to the rest of the maxilla by ridges of bone. This is similar to most basal archosauriforms, but some other erythrosuchids (and various more advanced archosauriforms) have thecodont teeth lacking this fusion. The teeth themselves are typical of carnivorous archosauriforms, being curved, blade-like, and serrated.