Kansas Geological Survey, Bulletin 202, part 3, originally published in 1971

Patrognathus and Siphonodella (Conodonta) from the Kinderhookian (Lower Mississippian) of Western Kansas and Southwestern Nebraska

by Gilbert Klapper

Originally published in 1971 as Kansas Geological Survey Bulletin 202, part 3. This is, in general, the original text as published. The information has not been updated.

Abstract

Late Kinderhookian conodont faunas occur in the subsurface of Kansas and Nebraska. Patrognathus andersoni is a new species that is associated with late Kinderhookian phylogenetic developments of Siphonodella in a well core from Logan County, Kansas, and also 300 feet above the base of the Lodgepole Limestone at Browns Gulch, Montana. Other occurrences of P. andersoni in the subsurface and in the Gilmore City Limestone of Iowa appear to be stratigraphically higher than the Siphonodella succession, but are assumed to be late Kinderhookian in the absence of evidence to the contrary.

Plates

The two plates are also available as a higher-resolution Acrobat PDF file (9.5 MB).

Introduction

Late Kinderhookian (Early Mississippian) strata in wells in western Kansas and southwestern Nebraska (Fig. 1) have yielded small conodont faunas. Strata assigned to the Gilmore City Limestone (Goebel, 1968, p. 1746) in Sinclair No. 1 Mercer and Mobil No. 1 Hogsett cores (loc. 1 and 3; Locality Register, p. 6) contain a fauna dominated by Patrognathus andersoni sp. nov. The specimens from the Mercer core were previously identified as ?Scaphignathus (Goebel, 1968, p. 1746, following my suggestion that the form in question was not Scaphignathus Helms) and later as Clydagnathus n. sp. B (Klapper et al., 1971, p. 309). The Mercer and Hogsett forms, however, constitute a new species, Patrognathus andersoni, distinct from species of Clydagnathus. Patrognathus andersoni also occurs in the type Gilmore City Limestone of Iowa (Anderson, 1969), supporting the physical correlation of strata in the Mercer and Hogsett wells with the Iowa formation.

Figure 1--Index map showing sample localities, state capitals, and Gilmore City, Iowa. Localities 1, 2, and 3 are cores; 4, 5, and 6 are surface samples.

The purpose of the present report, therefore, is to describe Patrognathus andersoni from the Mercer and Hogsett cores and its additional occurrence with species of Siphonodella in the Texas No. 1 Smith (loc. 2; Locality Register). The latter core provides a means of relating P. andersoni to the better known Siphonodella sequence and an opportunity to review the Systematics of late Kinderhookian species of Siphonodella.

Acknowledgments

I am grateful to Edwin D. Goebel, State Geological Survey of Kansas, Lawrence, who furnished the conodont faunas from the Kansas and Nebraska cores. Charles A. Sandberg, U. S. Geological Survey, Denver, graciously led me to the two Montana Lodgepole Limestone localities (loc. 4 and 5, see Locality Register). H. Richard Lane, Amoco Production Company, Tulsa, loaned conodonts collected by Alan B. Shaw from the Lodgepole at Browns Gulch, Blaine County, Montana. I am grateful to G. NI. Philip, University of New England, Armidale, New South Wales, Australia, for discussing aspects of Siphonodella taxonomy.

Faunal Analysis

The Upper Mississippi Valley Kinderhookian conodont sequence has been discussed by Collinson et al. (1962), who listed faunas from northern and central Missouri and western Illinois sections. The upper Kinderhookian and Osagian conodont successions on the southern flank of the Ozark uplift in southwestern Missouri, northern Arkansas, and northeastern Oklahoma have been described in detail by Thompson and Fellows (1970). The phylogenetic lineages of species of Siphonodella (Collinson et al., 1962, chart 2), which are partially duplicated in Wyoming sections (Sandberg and Klapper, 1967), are among the key aspects of the Kinderhookian sequence.

Heretofore, Patrognathus andersoni has not been linked to the Siphonodella succession, but three localities now provide evidence on the relative stratigraphic position of this species. Patrognathus andersoni occurs at 5188 feet in the Texas No. 1 Smith well (loc. 2, Table 1) above samples in the core with Siphonodella quadruplicata, S. cooperi, S. obsoleta, S. isosticha, and S. cf. S. isosticha and below samples with the same five form species. This association suggests that in the Texas No. 1 Smith, P. andersoni is of late Kinderhookian age, at least as young as the Siphonodella sandbergi-S. duplicata Zone (Sandberg and Klapper, 1967; Thompson and Fellows, 1970, Table 1) and most likely younger.

Table 1--Distribution and number of conodonts in the Texas No. 1 Smith (loc. 2).

Patrognathus andersoni occurs in association with Siphonodella isosticha at 303 feet above the base of the Lodgepole Limestone at Browns Gulch, Montana (NE NE SW sec. 11, T. 26 N., R. 24 E., Blaine County), 65 feet below an occurrence of S. isosticha and S. cf. S. isosticha. A fauna of the Lower Siphonodella crenulata Zone is found in the basal 5 feet of the Lodgepole Limestone at nearby Little Chief Canyon (Sandberg and Klapper, 1967, p. B43; N2 sec. 30, T. 26 N., R. 25 E., shown on pl. 52, Knechtel, 1959). A third association of P. andersoni with Siphonodella is the occurrence with S. Cooperi in Tournaisian (Tn1b) strata in Belgium (Austin et al., 1970).

Patrognathus andersoni occurs in small faunas without Siphonodella in the Sinclair No. 1 Mercer and the Mobil No. 1 Hogsett wells (loc. 1, 3; Table 2). These cores are not strictly datable by conodonts for one cannot assume that P. andersoni does not range above Siphonodella. Indeed, Goebel (1968, fig. 12, wells no. 18 and 22) indicates by physical correlation that the conodont samples of the Mercer core are higher than the Siphonodella-bearing samples of the Texas No. 1 Smith.

Table 2--Distribution and number of conodonts in the Sinclair No. 1 Mercer (loc. 1) and the Mobil No. 1 Hogsett (loc. 3).

The same relationship of Patrognathus andersoni above the Siphonodella sequence appears to exist in northern and central Iowa, where P. andersoni occurs in the type Gilmore City Limestone without Siphonodella (the upper 4 feet of the Streptorhynchus Zone of Laudon, 1933, p. 11; Anderson, 1969, pl. 109, fig. 1, 3, 4, 6). According to Laudon (1931, p. 432) and Anderson (1969, fig. 1, loc. 1 and 5), the Gilmore City is considered to be at a stratigraphic position well above the Maynes Creek Member of the Hampton Formation in the LeGrand area (the upper 2 feet of the Maynes Creek at loc. 5, Anderson, 1969, pl. 109, fig. 12, 23, has yielded Siphonodella crenulata).

In summary, the Kansas (Texas No. 1 Smith) and Montana (Browns Gulch) occurrences of Patrognathus andersoni are with late Kinderhookian species of Siphonodella, whereas the occurrences of P. andersoni above Siphonodella may be tentatively assumed to be slightly younger, but not as young as earliest Osagian (the Gnathodus semiglaber-Polygnathus communis carina Zone of the Pierson Formation, Thompson and Fellows, 1970).

Locality Register

Loc. 1--Sinclair Oil Co. No. 1 Mercer, sec. 28, T. 10 S., R. 40 W., Sherman County, Kansas. Well no. 18, Goebel, 1968, Table 1 and fig. 12.

Loc. 2--Texas Company No. 1 Smith, sec. 30, T. 11 S., R. 36 W., Logan County, Kansas. Well no. 22, Goebel, 1968, Table 1 and fig. 12.

Loc. 3--Mobil Oil Co. No. 1 Hogsett, sec. 12, T. 5 N., R. 41 W., Chase County, Nebraska. Well no. 26, Hilpman, 1969, Table 1.

Loc. 4--Bandbox Mountain, NE NW sec. 20, T. 14 N., R. 10 E., Judith Basin County, Montana.

Loc. 5--Red Hill, NE SE sec. 22, T. 2 N., R. 3 W., Jefferson Island quadrangle, Jefferson County, Montana.

Loc. 6--Browns Gulch, NE NE SW sec. 11, T. 26 N., R. 24 E., Blaine County, Montana.

Explanation of Plate 1

All figures are X40

Figures 1-10--Patrognathus andersoni sp. nov. 1, lateral, 2, lower, 3, upper views of KUMIP Holotype 1,800,684; loc. 1, 5475 feet; 4, lateral, 5, lower, 6, upper views of KUMIP Paratype 1,800,685; loc. 1, 5475 feet; 7, upper, 8, lower, 9, lateral views of KUMIP Paratype 1,800,686; loc. 1, 5460 feet; 10, upper view of KUMIP Paratype 1,800,687; loc. 3, 5355 feet.

Figures 11, 12--Polygnathus inornatus sensu Branson and Mehl. 11, lower, 12, upper views of KUMIP 1,800,688; loc. 2, 5193 feet.

Figures 13-15, 21--Siphonodella cooperi Hass. 13, 14, upper views of SUI 35137, 35138; loc. 4, 0-0.2 feet above base of Lodgepole Limestone; 15, upper, 21, lower views of SUI 35139; loc. 4, 0.2-0.5 feet above base of Lodgepole Limestone.

Figure 16--Siphonodella isosticha (Cooper). Upper view of UC Holotype 38975, originally illustrated by Cooper (1939, Pl. 41, fig. 9, 10) from the pre-Welden Shale of Oklahoma.

Figures 17-20--Siphonodella cf. S. isosticha (Cooper). 17, upper view of KUMIP 1,800,689; loc. 2, 5193 feet; 18, upper view of SUI 35222; loc. 4, 0-0.2 feet above base of Lodgepole Limestone; 19, upper view of SUI 35223; loc. 5, 2.7-3.6 feet above base of Lodgepole Limestone; 20, upper view of KUMIP 1,800,690; loc, 2, 5185 feet.

Figures 22-24--Siphonodella quadruplicata (Branson and Mehl). 22, upper view of KUMIP 1,800,691; loc. 2, 5185 feet; 23, upper view of KUMIP 1,800,692; loc. 2, 5193 feet; 24, upper view of SUI 35224; loc. 4, 0-0.2 feet above base of Lodgepole Limestone.

Figure 25--Siphonodella obsoleta Hass. Upper view of SUI 35225; loc. 4, 0-0.2 feet above base of Lodgepole Limestone.

Explanation of Plate 2

All figures are X40

Figures 1-3--Siphonodella cooperi Hass. 1, lower, 2, upper views of SUI 35226; loc. 4, 0.2-0.5 feet above base of Lodgepole Limestone; 3, upper view of KUMIP 1,800,693; loc. 2, 5185 feet.

Figures 4-14--Siphonodella crenulata (Cooper). 4, 5, 6, upper views of SUI 35227-35229; 7, lower, 8, upper views of SUI 35230; 9, upper view of SUI 35231; 10, lower, 11, upper views of SUI 35232; 12, lower, 13, upper views of SUI 35233. Fig. 4-8, 10-11 from loc. 4, 0-0.2 feet above base of Lodgepole Limestone; Fig. 9, 12, 13 from loc. 4, 0.2-0.5 feet above base of Lodgepole Limestone. 14, upper view of UC Holotype 39068, originally illustrated by Cooper (1939, pl. 41, fig. 1, 2) from the pre-Welden Shale of Oklahoma.

Systematic Paleontology

Kansas and Nebraska specimens (loc. 1-3) are reposited in the University of Kansas Museum of Invertebrate Paleontology (KUMIP). Montana specimens (loc. 4, 5) are reposited in the University of Iowa collections (SUI). Types originally figured by Cooper (1939) and reillustrated here are housed in the Field Museum of Natural History (Nitecki and Richardson, 1967, p. 3; numbers following abbreviation UC in plate explanations). The abbreviation, ICZN, used in the Systematics refers to the International Code of Zoological Nomenclature.

Material from the three Kansas and Nebraska cores is not adequate for multielement analysis, but all form species recovered are listed in Tables 1 and 2.

Genus POLYGNATHUS Hinde, 1879

Polygnathus HINDE, 1879, p. 361-362.
Type species--Polygnathus dubius HINDE, 1879, p. 362-364 (=P. foliatus BRYANT, lectotype of which was chosen as neotype of P. dubius by HUDDLE, 1970, p. 1037).

POLYGNATHUS DISTORTUS Branson and Mehl

Polygnathus distorta BRANSON AND MEHL, 1934, p. 294, pl. 24, fig. 12.
Polygnathus inornata E. R. Branson. KLAPPER, 1966, p. 19-20, pl. 1, fig. 11, 12 [only]; pl. 4, fig. 3 [only].
[non] Siphonodella distorta (Branson and Mehl). STRAKA, 1968, p. 41, pl. 4, fig. 10 (=Siphonodella sandbergi Klapper).
Polygnathus distortus Branson and Mehl. DRUCE, 1969, p. 96, pl. 24, fig. 1.
Polygnathus inornatus lobatus Branson and Mehl. THOMPSON AND FELLOWS, 1970, p. 95, pl. 3, fig. 12, 16, 19.

Remarks--Polygnathus distortus has a characteristic platform outline that serves to distinguish it from P. inornatus E. R. Branson. The posterior end is bluntly terminated in a round, convex curve in P. distortus, whereas the termination is sharply pointed with a sinus just to the anterior in the outer margin of P. inornatus. Additionally, P. distortus is characterized by two strong anterior rostral ridges on the left side of the platform and a deep and long outer adcarinal groove.

POLYGNATHUS INORNATUS Branson

Polygnathus inornata E. R. BRANSON, 1934, p. 309, pl. 25, fig. 8, 26; KLAPPEFI, 1966, p. 19-20, pl. 1, fig. 9, 10, 13, 14 [only]; STRAKA, 1968, p. 30-32, pl. 2, fig. 4, 5, 8; pl. 5, fig. 1, 3, 4, 5, 7.
Polygnathus lobata BRANSON AND MEHL, 1938, p. 146, pl. 34, fig. 44-47; REXROAD AND SCOTT, 1964, p. 35-36, pl. 2, fig. 15, 16; CANIS, 1968, p. 544-545, pl. 72, fig. 8.
Polygnathus lobatus lobatus Branson and Mehl. RHODES et al., 1969, p. 191-192, pl. 9, fig. 5-8.
Polygnathus lobatus inflexus RHODES et al., 1969, p. 192, pl. 9, fig. 9.
Polygnathus inornatus vexatus RHODES et al., 1969, p. 187-188, pl. 10, fig. 1, 3 [only].
Polygnathus lobatus Branson and Mehl. REXROAD, 1969, p. 35, pl. 5, fig. 16-18; AUSTIN AND RHODES, 1970, in Austin et al., p. 314, pl. 1, fig. 22.
Polygnathus inornatus inornatus Branson. THOMPSON AND FELLOWS, 1970, p. 94-95, pl. 3, fig. 2, 4, 17, 18.

Lectotype--The specimen illustrated by E. R. Branson (1934, pl. 25, fig. 8) is herewith selected as lectotype of Polygnathus inornatus.

Remarks--A number of authors have attempted to distinguish Polygnathus inornatus from P. lobatus on the supposed presence in the latter of a lobe in the posterior outer margin. What Branson and Mehl (1938, p. 146) called "a marked tendency toward the development of a postero-laterally extending point or lobe" in the posterior outer margin is not, with one exception, a lobe as that term is used in conodont terminology (compare for example to Polygnathus glaber bilobatus Ziegler, 1962, pl. 10, fig. 4, 16, 21). Of the original specimens of P. lobatus Branson and Mehl (1938, pl. 34, fig. 44-47) only the one represented by fig. 45 has a lobe. References to P. lobatus by later authors conform to Branson and Mehl's specimens illustrated in their fig. 44, 46, 47 (fig. 47=holotype), which have a distinct constriction or sinus in the outer margin near the posterior termination of the platform. Exactly this same outline is present in E. R. Branson's types of P. inornatus. Polygnathus lobatus, thus, falls as a junior synonym of P. inornatus E. R. Branson.

Although this synonymy was advocated earlier (Voges, 1959, p. 291; Klapper, 1966, p. 19-20), I additionally followed E. B. Branson and Mehl (1934, pl. 24, fig. 5-7) in referring their specimens, and similar forms, to P. inornatus. It now seems clear that P. inornatus of E. B. Branson and Mehl is different from P. inornatus E. R. Branson, as follows: the former has a virtually straight blade and carina that divide an almost bilaterally symmetrical platform, whereas P. inornatus E. R. Branson has an asymmetrical platform, with a sinus in the posterior outer margin and characteristically a sinuous posterior carina. Both forms have a short free blade and strongly upturned anterior margins.

POLYGNATHUS INORNATUS sensu Branson and Mehl

Pl. 1, fig. 11, 12

Polygnathus inornata E. R. Branson. BRANSON AND MEHL, 1934 p. 293, pl. 24, fig. 5-7; REXROAD AND SCOTT, 1964, p. 35, pl 2, fig. 19, 20; KLAPPER, 1966, p. 19-20, pl. 4, fig. 2, 4 [only]; CANIS, 1968, p. 544, pl. 72, fig. 25; STRAKA, 1968, p. 30-32, pl. 1, fig. 16, 17; pl. 5, fig. 6, 8 [only].
Polygnathus symmetrica Branson. STRAKA, 1968, p. 35, pl. 1, fig. 11, 13 [only].
Polygnathus inornatus inornatus Branson and Mehl [sic]. RHODES et al., 1969, p. 186, pl. 10, fig. 4-6; DRUCE, 1969, p. 98, pl. 20, fig. 1-3.

Remarks--The question of the authorship of Polygnathus inornatus is critical, if, in fact, E. B. Branson and Mehl's Bushberg specimens belong to a different form species from E. R. Branson's Hannibal specimens, as newly advocated here. Branson and Mehl (1934, p. 293) cited E. R. Branson as author, but this is not sufficient according to Art. 50 (ICZN), for their differentiation of P. inornatus from P. longiposticus would have validated P. inornatus had E. R. Branson s paper never been published. Both papers, however, were published simultaneously as part of the fourth number of Vol. 8 of the University of Missouri Studies. Neither author(s) has priority until the action of the "first reviser," which would determine the relative priority of authorship [Art. 24(a), ICZN, which surely must apply to authorship as well as to synonyms]. Here, I construe "first reviser" to mean the first author after 1934 who placed E. B. Branson and Mehl's Bushberg specimens in synonymy with E. R. Branson's Hannibal specimens. The first revisers are E. B. Branson and Mehl (1938, p. 146) who referred one of the original Hannibal (pl. 33, fig. 15) and two of the original Bushberg (pl. 33, fig. 51, 52) specimens to P. inornatus and again cited E. R. Branson as author. Cooper's action (1939, p. 400) is identical. Therefore, E. R. Branson is the author of P. inornatus, and page precedence in the original volume has no relevance.

Consequently, Polygnathus inornatus sensu Branson and Mehl is left without a name. It is possible that a name introduced either by Cooper (1939) or Youngquist and Patterson (1949) might apply equally to the specimens under discussion, but this is not confirmed as yet.

Genus PATROGNATHUS Rhodes, Austin, and Druce, 1969

Patrognathus RHODES et al., 1969, p. 178-179.
Type species--Patrognathus variabilis RHODES et al., 1969, p. 179-180, pl. 2, fig. 8-11.

Remarks--Patrognathus has a longer free blade than that of Clydagnathus Rhodes et al. (1969) and lacks a fixed blade, whereas in Clydagnathus at least one denticle, and more commonly two or three comprise a fixed blade. The anterior blade denticles of Patrognathus are more or less uniform in height or rise gradually to the posterior (in front of the high posteriormost denticle). Characteristically the blade denticles of Clydagnathus decline abruptly to the anterior. The anterior part of the blade is medial in Patrognathus, but characteristically is on the right side in Clydagnathus.

Rhodes et al. (1969, p. 178) regarded Patrognathus as broadly homeomorphic with Taphrognathus Branson and Mehl and Streptognathodus Stauffer and Plummer [in the context of their reference to Rexroad (1958), I assume that the Chesteran (Upper Mississippian) form now called Adetognathus unicornis (Rexroad and Burton) was the intended citation]. Patrognathus, then represented only by P. variabilis, was distinguished by Rhodes et al. from Taphrognathus on the basis of the wider basal cavity in the former. Yet some specimens of T. varians Branson and Mehl (e.g., Thompson and Goebel, 1969, pl. 5, fig. 7, 8) have almost as wide a cavity as P. variabilis. With the inclusion in Patrognathus of P. andersoni sp. nov., which has a narrow cavity comparable to that of Taphrognathus, other means of distinguishimg the two genera must be sought. Taphrognathus, as characterized by its type, and perhaps only named species, T. varians, has a long free blade that declines gradually to the posterior and a short fixed blade that lies between the lateral margins (see Branson and Mehl, 1941, pl. 6, fig. 27-41; Thompson and Goebel, 1969, pl. 5, fig. 1-9, 12-15). In contrast, both P. variabilis and P. andersoni have the highest denticle at the posterior end of the free blade and both lack a fixed blade. Taphrognathus capricornis Druce (1970, p. 102, pl. 15, fig. 3-5) seemingly is more closely related morphologically to P. andersoni than to T. varians and perhaps represents a younger representative of Patrognathus.

Patrognathus andersoni sp. nov.

Pl. 1, fig. 1-10

Patrognathus variabilis Rhodes, Austin, and Druce. ANDERSON, 1969, p. 922, pl. 109, fig. 1, 3, 4, 6; AUSTIN AND RHODES, 1970, in Austin et al., p. 314, pl. 1, fig. 7.

Derivation of name--The species is named for my friend and colleague, Dr. Wayne I. Anderson.

Holotype--KUMIP 1,800,684, the specimen illustrated on Pl. 1, fig. 1-3.

Type locality--Sinclair Oil Co. No. 1 Mercer, loc. 1.

Type stratum--5475 feet (core depth).

Diagnosis--Representative specimens of Patrognathus andersoni have a medial free blade, except that the high and broad posteriormost denticle is twisted to the right side. A distinct medial trough on the platform may or may not be present. The basal cavity is relatively narrow.

Description--The free blade is composed of about five to eight denticles, which except for the posteriormost high denticle are more or less uniform in height or rise gradually to the posterior. The posteriormost denticle of the free blade is markedly higher and broader than the rest; it terminates in front of the lateral margins of the platform. In some specimens, a medial trough separates the lateral margins, which bear round nodes. In other specimens a narrow gap separates the marginal nodes anteriorly, but the nodes join posteriorly. The posterior lower margin is only slightly arched. The basal cavity occupies the entire area beneath the platform and tapers to the posterior end.

Remarks--Patrognathus andersoni has a much narrower basal cavity as compared to the greatly expanded cavity seen in the original illustrations of P. variabilis Rhodes et al. (1969, pl. 2, fig. 8-11) and in the specimen from the upper tongue of the Cottonwood Canyon Member of the Madison Limestone at Windy Gap, Wyoming (Sandberg and Klapper, 1967, p. B52, cited as n. gen., n. sp. Rhodes, Austin, and Druce). Later references to P. variabilis are included here in P. andersoni (see synonymy). Patrognathus variabilis does not have as well developed a medial trough as in some specimens of P. andersoni.

Patrognathus andersoni may be distinguished from Adetognathus unicornis (Rexroad and Burton, 1961, p. 1157, pl. 138, fig. 1-9; Lane, 1967, p. 930-931, pl. 119, fig. 16-21), which has a deeper and longer trough flanked by transverse ridges on the lateral margins. Furthermore, A. unicornis has the free blade attached either to the right or to the left margin of the platform, whereas the anterior free blade of P. andersoni is medial and the posteriormost blade denticle is twisted to the right side.

Patrognathus andersoni is distinguished from Taphrognathus capricornis Druce (1970, p. 102, pl. 15, fig. 3-5) especially by the lateral outlines of the lower margin and the upper margin of the free blade.

Genus SIPHONODELLA Branson and Mehl, 1944

Siphonognathus BRANSON AND MEHL, 1934, p. 295 [non RICHARDSON, 1858, fide Branson and Mehl, 1948, p. 528].
Siphonodella BRANSON AND MEHL, 1944, in Shimer and Shrock, p. 245 [pro Siphonognathus].

Type species--Siphonognathus duplicata BRANSON AND MEHL, 1934, p. 296-297, pl. 24, fig. 16, 17 (original designation).

SIPHONODELLA COOPERI Hass

Pl. 1, fig. 13-15, 21; Pl. 2, fig. 1-3

Siphonodella cooperi HASS, 1959, p. 392-393, pl. 48, fig. 35, 36; HIGGINS, 1964, in Higgins et al., p. 225, pl. 5, fig. 31; KLAPPER, 1966, p. 16, pl. 2, fig. 10, 11; pl. 3, fig. 1-4; ADRICHEM BOOGAERT, 1967, p. 186, pl. 3, fig. 14; STRAKA, 1968, p. 39-40, pl. 3, fig. 10, 11; pl. 6, fig. 10, 12, 13, 16 [only]; DRUCE, 1969, p. 119-120, pl. 39, fig. 3, 4; ANDERSON, 1969, p. 924, pl. 108, fig. 1, 2, 10, 11; MATTHEWS, 1969, p. 279, pl. 51, fig. 9, 14, 15; SCHÖNLAUB, 1969, P. 343-344, pl. 2, fig. 8; REXROAD, 1969, p. 41-42, pl. 3, fig. 10, 11, 13; AUSTIN AND RHODES, 1970, in Austin et al., p. 314, pl. 1, fig. 9 [fig. 8=?].
Siphonodella duplicata (Branson and Mehl). STRAKA, 1968, p. 42, pl. 6, fig. 14, 15; SPASSOV et al., 1968, p. 163, pl. 3, fig. 2.

Diagnosis--In representative specimens of Siphonodella cooperi the longest rostral ridge either curves out to terminate posteriorly at midlength of the outer margin or it forms that margin throughout its course. Number of rostral ridges varies from two to three. Outer posterior platform bears transverse ridges, inner platform is nodose.

Remarks--The division of S. cooperi into subspecies (Thompson and Fellows, 1970, p. 104-105) is not accepted because illustrated types of S. cooperi hassi are referable either to S. obsoleta or S. isosticha (see respective synonymies).

SIPHONODELLA CRENULATA (Cooper)

Pl. 2, fig. 4-14

Siphonognathus crenulata COOPER, 1939, p. 409, pl. 41, fig. 1, 2 [reillustrated here on Pl. 2, fig. 14].
Siphonodella crenulata (Cooper). VOGES, 1959, p. 307-308, pl. 35, fig. 23-30; KLAPPER, 1966, p. 18, pl. 3, fig. 5-8 [synonymy to 1966]; REXROAD, 1969, p. 42, pl. 2, fig. 9, 10; THOMPSON AND FELLOWS, 1970, p. 105-106, pl. 6, fig. 7, 10.
Siphonodella obsoleta Hass. ANDERSON, 1969, p. 924-925, pl. 109, fig. 12, 23 [only].
Siphonodella isosticha (Cooper). MATTHEWS, 1969, p. 279-280, pl. 51, fig. 5 [only].

Diagnosis--Representative specimens of Siphonodella crenulata have a markedly asymmetrical platform outline. Outer margin characteristically crenulate, inner margin may have a sharp angular bend at midlength. Two short rostral ridges; only exceptionally are there three. In mature specimens, outer posterior platform bears weak transverse ridges, inner platform is nodose.

Remarks--A growth series of Siphonodella crenulata is illustrated (Pl. 2, fig. 4-13) from the Lodgepole Limestone at Bandbox Mountain, Montana (loc. 4). juvenile specimens of this series have a relatively smooth posterior platform, although a row of nodes parallel and adjacent to the carina may form on the outer side. The platform outline of S. crenulata distinguishes it from other species. The specimens of Schönlaub (1969, pl. 2, fig. 4, 5) do not appear to belong to S. crenulata, because of differences in platform outline and ornament.

SIPHONODELLA ISOSTICHA (Cooper)

Pl. 1, fig. 16

Siphonognathus isosticha COOPER, 1939, p. 409, pl. 41, fig. 9, 10 [reillustrated here on Pl. 1, fig. 16].
Siphonodella obsoleta Hass. KLAPPER, 1966, p. 17, pl. 2, fig. 9, 12 [only]; ADRICHEM BOOGAERT, 1967, p. 186, pl. 3, fig. 15.
Siphonodella isosticha (Cooper). RHODES et al., 1969, p. 220, pl. 12, fig. 9, 11; DRUCE, 1969, p. 121, pl. 39, fig. 7, 8 [only]; REXROAD, 1969, p. 43, pl. 3, fig. 1, 2.
Siphonodella cooperi hassi THOMPSON AND FELLOWS, 1970, p. 105, pl. 6, fig. 1, 3, 5 [only].

Diagnosis--In representative specimens of Siphonodella isosticha the posterior termination of the longest rostral ridge is at the outer platform margin, opposite the position where the carina begins to incurve. Outer posterior platform smooth to weakly nodose, inner platform nodose.

Remarks--Study of the holotype of Siphonodella isosticha (Pl. 1, fig. 16) shows that the inner posterior platform is weakly nodose and that the longest rostral ridge terminates at the outer margin. In some small specimens the longest rostral ridge forms the outer margin. The diagnosis of S. isosticha given by Thompson and Fellows (1970, p. 107) applies to specimens in which the longest rostral ridge terminates on the platform rather than at the margin; such specimens are here referred to S. cf. S. isosticha.

SIPHONODELLA cf. S. ISOSTICHA (Cooper)

Pl. 1, fig. 17-20

Siphonodella obsoleta Hass. VOCES, 1959, p. 309-310, pl. 35, fig. 48-50.
Siphonodella isosticha (Cooper). REXROAD AND SCOTT, 1964, p. 44, pl. 3, fig. 21, 23; ETHINGTON, 1965, p. 587, pl. 67, fig. 17 [only]; CANIS, 1968, p. 549, pl. 72, fig. 9; DRUCE, 1969, p. 121, pl. 39, fig. 9 [only]; SCHÖNLAUB, 1969, p. 345, pl. 2, fig. 14; REXROAD, 1969, p. 43, pl. 3, fig. 3 [only]; THOMPSON AND FELLOWS, 1970, p. 106-107, pl. 6, fig. 8, 9, 13, 14.

Diagnosis--In representative specimens of Siphonodella cf. S. isosticha the posterior termination of the longest rostral ridge on the outer platform is adjacent to the position where the carina begins to incurve and midway between the margin and the carina. Long rostral ridge on inner side terminates at a comparable position. Posterior platform ornament weakly nodose on both sides, but somewhat stronger on the inner side.

Remarks--This category receives specimens formerly referred to S. isosticha, but differs from that species in having the longest rostral ridge terminate on the platform rather than at the outer margin. Although this difference may seem relatively minor, nevertheless two discrete morphological groups are recognizable.

SIPHONODELLA OBSOLETA Hass

Pl. 1, fig. 25

Siphonodella duplicata (Branson and Mehl). YOUNGQUIST AND PATTERSON, 1949, p. 69, pl. 16, fig. 10 [only].
Siphonodella obsoleta HASS, 1959, p. 392-393, pl. 47, fig. 1, 2; VOGES, 1959, p. 309-310, pl. 35, fig. 40-47; ZIEGLER, 1960, in Kronberg et al., pl. 3, fig. 8; CONIL, 1964, pl. 12, fig. 14; KLAPPER, 1966, p. 17, pl. 4, fig. 17, 19 [only]; SPASSOV, 1966, p. 96, pl. 1, fig. 17; CANIS, 1968, p. 550, pl. 72, fig. 11; STRAKA, 1968, p. 42-43, pl. 4, fig. 2, 3; RHODES et al., 1969, p. 220-221, pl. 12, fig. 13; ANDERSON, 1969, p. 924- 925, pl. 108, fig. 3, 5 [only]; SCHÖNLAUB, 1969, p. 345-346, pl. 2, fig. 13; REXROAD, 1969, p. 44, pl. 3, fig. 6.
Siphonodella isosticha (Cooper). ETHINGTON, 1965, p. 587, pl. 67, fig. 15 [only]; DRUCE, 1969, p. 121, pl. 39, fig. 5 [only].
Siphonodella cooperi Hass. THOMPSON, 1967, p. 52, pl. 5, fig. 18, 19 [only].
Siphonodella trirostrata DRUCE, 1969, p. 123-124, pl. 41, fig. 8 [only].
Siphonodella cooperi hassi THOMPSON AND FELLOWS, 1970, p. 105, pl. 6, fig. 2, 4 [only].

Diagnosis--Representative specimens of Siphonodella obsoleta have a long rostral ridge that extends to near the posterior end of the outer platform. Outer posterior platform weakly ornamented or smooth between the long rostral ridge and carina. Rostral ridges vary from two to four in number; platform is long and relatively narrow.

Remarks--The paratype of S. trirostrata DRUCE (1969, pl. 41, fig. 8) and a paratype of S. cooperi hassi Thompson and Fellows (1970, pl. 6, fig. 2, 4) do not differ appreciably from S. obsoleta. The specimen of Youngquist and Patterson (1949) in the slide labeled as SUI 4145, Pl. 16, fig. 8, is actually the specimen illustrated in Pl. 16, fig. 10 and is an S. obsoleta. The specimen in the slide labeled as SUI 4146, Pl. 16, fig. 9, 10, is the specimen illustrated in fig. 8, 9, although the heavy retouching of the photographs has obscured the transverse ridges on the outer platform and other details. The latter specimen is S. cooperi. This interpretation differs from the earlier comments and synonymy lists of Klapper (1966, p. 16, 17) and the discussion of Rexroad (1969, p. 44).

SIPHONODELLA QUADRUPLICATA (Branson and Mehl)

Pl. 1, fig. 22-24

Siphonognathus quadruplicata BRANSON AND MEHL, 1934, p. 295-296, pl. 24, fig. 18-20 [non fig. 21=S. cooperi].
Siphonodella quadruplicata (Branson and Mehl). BRANSON AND MEHL, 1944, in Shimer and Shrock, p. 245, pl. 94, fig. 44, 45; KLAPPEIR 1966, p. 17-18, pl. 2, fig. 5-8; pl. 3, fig. 9-12; pl. 4, fig. 16, 20 [synonymy to 1966]; CANIS, 1968, p. 550, pl. 72, fig. 2; STRAKA, 1968, p. 43-45, pl. 2, fig. 10, 11; pl. 3, fig. 2, 6-8; pl. 4, fig. 9, 11; DRUCE, 1969, p. 121-122, pl. 40, fig. 1-3; ANDERSON, 1969, p. 925, pl. 108, fig. 4, 6-9, 12; SCHÖNLAUB, 1969, p. 346, pl. 2, fig. 15; REXROAD, 1969, p. 44-45, pl. 2, fig. 11, 12; THOMPSON AND FELLOWS, 1970, p. 108-109, pl. 8, fig. 3-7.
Siphonodella duplicata (Branson and Mehl) var. A HASS, 1956, p. 25, pl. 2, fig. 23 [only]; CLOUD, BARNES, AND HASS, 1957, p. 809, pl. 5, fig. 8.
Siphonodella crenulata (Cooper). REXROAD AND SCOTT, 1964, p. 44, pl. 3, fig. 26; CANIS, 1968, p. 548, pl. 72, fig. 21.
Siphonodella duplicata (Branson and Mehl). MANZONI, 1966, p. 484, pl. 60, fig. 2; CANIS, 1968, p. 548-549, pl. 72, fig. 3, 4, 7.
Siphonodella cf. S. crenulata (Cooper). STRAKA, 1968, p. 40-41, pl. 2, fig. 9, 12.
Siphonodella trirostrata DRUCE, 1969, p. 123-124, pl. 41, fig. 7 [only].
Siphonodella cooperi cooperi Hass. THOMPSON AND FELLOWS, 1970, p. 104-105, pl. 6, fig. 15, 17 [only].

Diagnosis--In representative specimens of Siphonodella quadruplicata the posterior termination of the innermost rostral ridge on the outer platform is adjacent to the position where the carina begins to incurve and between the margin and the carina. Number of rostral ridges varies from three to five. Outer posterior platform bears transverse ridges, inner platform is nodose.

Remarks--The distinction between Siphonodella quadruplicata and S. cooperi is based on the position of the posterior termination of the innermost rostral ridge on the outer platform, as emphasized in the respective diagnoses. Hass (1959, p. 392) used this character to distinguish S. cooperi from forms he had earlier called S. duplicata var. A. The latter have been interpreted (Klapper, 1966, p. 18) as early growth stages within the range of variation of S. quadruplicata and differ from representative specimens of S. duplicata (Branson and Mehl; e.g., see Hass, 1959, pl. 49, fig. 25), which have transverse ridges on both sides of the platform.

References

Adrichem Boogaert, H. A. van, 1967, Devonian and Lower Carboniferous conodonts of the Cantabrian Mountains (Spain) and their stratigraphic application: Leidse Geol. Mededelingen, v. 39, p. 129-192.

Anderson, W. I., 1969, Lower Mississippian conodonts from northern Iowa: Jour. Paleontology, v. 43, p. 916-928.

Austin, Ronald, Conil, Raphaël, Rhodes, Frank, and Streel, Maurice, 1970, Conodontes, spores et Foraminifères du Tournaisien inférieur dans la valleé du Hoyoux: Soc. Géol. Belgique Ann., v. 93, p. 305-313.

Branson, E. B., and Mehl, M. G., 1934, Conodonts from the Bushberg Sandstone and equivalent formations of Missouri : Univ. Missouri Studies, v. 8, no. 4, p. 265-299 [date of imprint, 19331.

Branson, E. B., and Mehl, M. G., 1938, Conodonts from the Lower Mississippian of Missouri; in, Stratigraphy and paleontology of the Lower Mississippian of Missouri, pt. 2, E. B. Branson, et al.: Univ. Missouri Studies, v. 13, no. 4, p. 128-148.

Branson, E. B., and Mehl, M. G., 1941, Conodonts from the Keokuk Formation: Denison Univ. Bull., v. 40, no. 14, Jour. Sci. Lab., v. 35, art. 6, p. 179-188 [date of imprint, 1940].

Branson, E. B., and Mehl, M. G., 1948, Conodont homonyms and names to replace them: Jour. Paleontology, v. 22, p. 527-528.

Branson, E. R., 1934, Conodonts from the Hannibal Formation of Missouri: Univ. Missouri Studies, v. 8, no. 4, P. 301-334 [date of imprint, 1933].

Canis, W. F., 1968, Conodonts and biostratigraphy of the Lower Mississippian of Missouri: Jour. Paleontology, v. 42, p. 525-555.

Cloud, P. E., Jr., Barnes, V. E., and Hass, W. H., 1957, Devonian-Mississippian transition in central Texas: Geol. Soc. America, Bull., v. 68, p. 807-816.

Collinson, Charles, Scott, A. J., and Rexroad, C. B., 1962, Six charts showing biostratigraphic zones, and correlations based on conodonts from the Devonian and Mississippian rocks of the Upper Mississippi Valley: Illinois State Geol. Survey, Circ. 328, 32 p.

Conil, Raphaël, 1964, Localités et coupes types pour l'étude du Tournaisien inférieur (Révision des limites sous l'aspect micropaléontologique): Acad. Roy. Belgique, Cl. Sci., Méinoires, v. 15, pt. 4, 87 p.

Cooper, C. L., 1939, Conodonts from a Bushberg-Hannibal horizon in Oklahoma: Jour. Paleontology, v. 13, p. 379-422.

Deuce, E. C., 1969, Devonian and Carboniferous conodonts from the Bonaparte Gulf Basin, northern Australia and their use in international correlation: Australia Bur. Mineral Resources, Bull. 98, 242 p.

Deuce, E. C., 1970, Lower Carboniferous conodonts from the northern Yarrol Basin, Queensland: Australia Bur. Mineral Resources, Bull. 108, p. 91-113.

Ethington, R. L., 1965, Late Devonian and Early Mississippian conodonts from Arizona and New Mexico: Jour. Paleontology, v. 39, p. 566-589.

Goebel, E. D., 1968, Mississippian rocks of western Kansas: Am. Assoc. Petroleum Geologists, Bull., v. 52, p. 17321778.

Hass, W. H., 1956, Age and correlation of the Chattanooga Shale and the Maury Formation: U.S. Geol. Survey, Prof. Paper 286, 47 p. [available online]

Hass, W. H., 1959, Conodonts from the Chappel Limestone of Texas: U.S. Geol. Survey, Prof. Paper 294-J, p. 365-399. [available online]

Higgins, A. C., Wagner-Gentis, C. H. T., and Wagner, R. H., 1964, Basal Carboniferous strata in part of northern León, N.W. Spain: stratigraphy, conodont and goniatite faunas: Soc. belge Géologie, Paléontologie, et Hydrologie Bull., v. 72, p. 205-248.

Hilpman, P. L., 1969, Devonian rocks in Kansas and their epeirogenic significance: Unpub. doctoral dissertation, Dept. Geology, Univ. Kansas, 73 p.

Hinde, G. J., 1879, On conodonts from the Chazy and Cincinnati Group of the Cambro-Silurian, and from the Hamilton and Genesee-Shale divisions of the Devonian, in Canada and the United States: Geol. Soc. London, Quart. Jour., v. 35, p. 351-369.

Huddle, T. W., 1970, Revised descriptions of some Late Devonian polygnathid conodonts: Jour. Paleontology, v. 44, p. 1029-1040.

International Commission on Zoological Nomenclature, 1961, International code of zoological nomenclature: Richard Clay and Co., Ltd. (Bungay, Suffolk), 176 p.

Klapper, Gilbert, 1966, Upper Devonian and Lower Mississippian conodont zones in Montana, Wyoming, and South Dakota: Univ. Kansas Paleont. Contr., Paper 3, 43 p. [available online]

Sandberg, C. A., Collinson, Charles, Huddle, J. W., Orr, R. W., Rickard, L. V., Schumacher, Dietmar, Seddon, George, and Uyeno, T. T., 1971, North American Devonian conodont biostratigraphy; in, Symposiuin on conodont biostratigraphy, W. C. Sweet and S. M. Bergström, (eds.): Geol. Soc. America, Mem. 127, p. 285-316.

Knechtel, M. M., 1959, Stratigraphy of the Little Rocky Mountains and encircling foothills, Montana: U.S. Geol. Survey, Bull. 1072-N, p. 723-752. [available online]

Kronberg, Peter, Pilger, Andreas, Scheiip, Adalbert, and Ziegler, Willi, 1960, Spuren altvariscischer Bewegungen im nordöstlichen Teil des Rheinischen Schiefergebirges; in, Das Karbon der subvariscischen Saumsenke, Ein Symposium, Teil 1, Der Kulm und die flözleere Fazies des Namurs: Fortschr. Geologie Rheinland u. Westfalen, Bd. 3, p. 1-46.

Lane, H. R., 1967, Uppermost Mississippian and Lower Pennsylvanian conodonts from the type Morrowan region, Arkansas: Jour. Paleontology, v. 41, p. 920-942.

Laudon, L. R., 1931, The stratigraphy of the Kinderhook Series of Iowa: Iowa Geol. Survey, Ann. Report, 1929, v. 35, p. 335-451.

Laudon, L. R., 1933, The stratigraphy and paleontology of the Gilmore City Formation of Iowa: Univ. Iowa Studies in Natural History, v. 15, no. 2, 74 p.

Manzoni, Marcello, 1966, Conodonti Neodevonici ed Eocarboniferi al Monte Zermula (Alpi Carniche): Giornale di Geologia, v. 33, p. 461-488.

Matthews, S. C., 1969, Two conodont faunas from the Lower Carboniferous of Chudleigh, south Devon: Palaeontology, v. 12, p. 276-280.

Nitecki, M. H., and Richardson, E. S., Jr., 1967, Catalog of type specimens of conodonts in the Field Museum of Natural History: Fieldiana: Geology, v. 17, no. 1, 101 p.

Rexroad, C. B., 1958, The conodont homeomorphs Taphrognathus and Streptognathodus: Jour. Paleontology, v. 32, p. 1158-1159.

Rexroad, C. B., 1969, Conodonts from the Jacobs Chapel bed (Mississippian) of the New Albany Shale in southern Indiana: Indiana Dept. Natural Resources, Geol. Survey Bull. 41, 55 p.

Rexroad, C. B., and Burton, R. C., 1961, Conodonts from the Kinkaid Formation (Chester) in Illinois: Jour. Paleontology, v. 35, p. 1143-1158.

Rexroad, C. B., and Scott, A. J., 1964, Conodont zones in the Rockford Limestone and the lower part of the New Providence Shale (Mississippian) in Indiana: Indiana Dept. Conservation, Geol. Survey Bull. 30, 54 p.

Rhodes, F. H. T., Austin, R. L., and Druce, E. C., 1969, British Avonian (Carboniferous) conodont faunas, and their value in local and intercontinental correlation: British Mus. (Nat. History) Bull., Geology, Suppl. 5, 313 p.

Sandberg, C. A., and Klapper, Gilbert, 1967, Stratigraphy, age, and paleotectonic significance of the Cottonwood Canyon Member of the Madison Limestone in Wyoming and Montana: U.S. Geol. Survey, Bull. 1251-B, p. BI-B70. [available online]

Schönlaub, H. P., 1969, Conodonten aus dem Oberdevon und Unterkarbon des Kronhofgrabens (Karnische Alpen, Österreich): Jahrbuch Geol. Bundesanstalt, v. 112, p. 321-354.

Shimer, H. W., and Shrock, R. R., 1944, Index fossils of North America: John Wiley and Sons, Inc. (New York), 837 p.

Spassov, Hristo, 1966, Significance of the conodont fauna for the stratigraphy of the Paleozoic: "Strasimir Dimitrov" Inst. Geol. Bull., v. 15, p. 89-97.

Stojanovic-Kuzenko, Smiljana, and Pajic, Vera, 1968, Les nouveaux résultats obtenus par l'étude des Conodontes Paléozoïques de ]a Serbie du nord-ouest: Inst. Recherches Géol. et Géophysiques, v. 26, p. 153-166.

Straka, J. J., 1968, Conodont zonation of the Kinderhookian Series, Washington County, Iowa: Univ. Iowa Studies in Natural History, no. 21, 71 p.

Thompson, T. L., 1967, Conodont zonation of Lower Osagean rocks (Lower Mississippian) of southwestern Missouri: Missouri Geol. Survey and Water Resources, Rept. Inv. 39, 88 p.

Thompson, T. L., and Fellows, L. D., 1970, Stratigraphy and conodont biostratigraphy of Kinderhookian and Osagean rocks of southwestern Missouri and adjacent areas: Missouri Geol. Survey and Water Resources, Rept. Inv. 45, 263 p.

Thompson, T. L., and Goebel, E. D., 1968, Conodonts and stratigraphy of the Meramecian Stage (Upper Mississippian) in Kansas: Kansas Geol. Survey, Bull. 192, 56 p. [available online]

Voges, Adolf, 1959, Conodonten aus dem Unterkarbon I und II (Gattendorfia- und Pericyclus-Stufe) des Sauerlandes: Palëont. Zeitschr., Bd. 33, p. 266-314.

Youngquist, Walter, and Patterson, S. H., 1949, Conodonts from the Lower Mississippian Prospect Hill Sandstone of Iowa: Jour. Paleontology, v. 23, p. 57-73.

Ziegler, Willi, 1962, Taxionomie und Phylogenie Oberdevonischer Conodonten und ihre stratigraphische Bedeutung: Hessisches Landesamt Bodenforschung, Abh., no. 38, 166 p.

Kansas Geological Survey, Patrognathus and Siphonodella (Conodonta) from the Kinderhookian (Lower Mississippian) of Western Kansas and Southwestern Nebraska
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