«K03 S/ty/ NO tffl ^ .ssf* Digitized by the Internet Archive in 2012 with funding from Royal Ontario Museum http://archive.org/details/lowermiddledevonOOtelf ROYAL ONTARIO MUSEUM LIBRARIES RO M 3l76i 051 62375 9 Royal Ontario Museum 15 June 1977 Life Sciences Occasional Paper No. 30 Lower-Middle Devonian Conodont Biostratigraphy and Palaeoecology, Niagara Peninsula, Ontario P.G. Telford Ministry of Natural Resources, Ontario Division of Mines, Queen's Park, Toronto P.H. von Bitter Department of Invertebrate Palaeontology, Royal Ontario Museum, Toronto, Ontario G.A. Tarrant Department of Earth Sciences, University of Waterloo, Waterloo, Ontario Abstract Conodonts recovered from the Lower-Middle Devonian Bois Blanc Formation and Middle Devo- nian Edgecliff Member of the Onondaga Formation of southern Ontario demonstrate that the cono- dont fauna is uniform and of low diversity, containing the form genera lcriodus, Belodetla, Coelocerodontus, and Panderodus. Acodina, although possibly a component element of the apparatus of species of lcriodus, is rare. Two anomalous samples from the lower part of the Bois Blanc contain elements of a species of Ozarkodina. The conodont faunas suggest diachroneity of the Bois Blanc Formation and the unit may transgress the Lower-Middle Devonian boundary. The cherty, bioclas- tic limestones of the Bois Blanc Formation and Edgecliff Member were deposited on a broad shelf separating the Appalachian and Michigan basins. Very shallow water conditions are indicated by the macrofauna of profuse, colonial corals, and by development of biohermal or reefoid bodies. The conodont fauna therefore is part of a shallow-water community, equivalent perhaps to Druce's Bio- facies I or n. lcriodus is virtually ubiquitous but Belodella and Coelocerodontus show heterogeneities in distribution that possibly reflect variations in local environmental conditions, e.g., proximity to reefs. The absence of Polygnathus may confirm already proposed ecologic models of conodont dis- tribution in which this genus is placed in a different biofacies than is lcriodus. Introduction This study developed initially from the re- covery by von Bitter of abundant icriodid conodont elements from silicified carbonates collected at Hagersville, Ontario (Fig. 1, loc. 5). It progressed further as a result of re- gional mapping by Telford and Tarrant for the Ontario Division of Mines, involving strata of Late Silurian and Devonian age, in the Niagara Peninsula of southern Ontario (Fig. 1). Principal objectives of the mapping were precise definition of the Bois Blanc Formation, correlation of overlying carbo- nate units with either the Onondaga Forma- tion of the Appalachian Basin or the Ara- herstburg Formation of the Michigan Basin, and assessment of the magnitude of the sup- posed disconformity between the Bois Blanc and overlying units (Fig. 2). This field map- ping led Tarrant to study the distribution of conodonts at locality 2 in greater detail (Tar- rant, 1975). Best (1953) and Hewitt (1972) included all Devonian strata of the Niagara Peninsula in the Bois Blanc Formation. Oliver (1967) lim- ited the Bois Blanc to the lower part of the Devonian sequence and suggested correla- tion of the overlying strata with the Onon- daga Formation. Sanford (1969) also used a restricted definition of the Bois Blanc but equated the overlying strata with the Am- herstburg Formation. Recent mapping (Tel- ford and Tarrant, 1975a, 1975b) has con- firmed the restricted definition of the Bois Blanc, and supports Oliver's recognition of the Onondaga in the Niagara Peninsula. The lower 3-10 metres of the Onondaga in this area have been designated on lithological grounds as the Edgecliff Member as defined by Oliver (1954). Materials and Methods Sixty-eight samples were taken from the Bois Blanc Formation and Edgecliff Member at six localities in the Niagara Peninsula (Fig. 2). Reconnaissance samples were also ob- tained from the basal Bois Blanc from local- ity 7 at Innerkip and localities 8 and 9 along Sample locality Bois Blanc Formation Fig. I Conodont sample localities and surface outcrop distribution of Bois Blanc Formation, southwestern Ontario. J s J £ a. 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However, morphological transitions ob- served in specimens in several samples, as for example in sample C9201, suggest that all the icriodiform elements are referable to the subspecies, Icriodus latericrescens robus- tus Orr. Specimens range from very small elements with no lateral processes (superfi- cially similar to /. angustus Stewart and Sweet, as illustrated in Klapper and Ziegler, 1967, pi. 10, figs. 1-3), through slightly larger elements with one incipient lateral process, to elements with one well-developed lateral process (identical with /. latericrescens robustus of Orr, 1971, pi. 2, figs. 14-15), and finally to large elements with an expanded posterior area containing a large denticu- lated lateral process opposite a prominent but shorter nondenticulated lateral process. The end member of this gradational series resembles /. latericrescens bilatericrescens Ziegler. In Table 1 the elements lacking processes are referred to as "simple"; those with one process are termed "intermediate"; and those with two processes are termed "advanced". Numerous broken specimens that could be identified to subspecific level by features other than the processes, e.g., denticulation, are placed in the category "fragmentary". Specimens of /. latericrescens robustus studied by Tarrant have not been subdivided in this manner (Table 2). A further morphological variation occurs between specimens of /. latericrescens robustus from the Niagara Peninsula and those from the Innerkip and Teeswater River regions. The former are relatively long units with a parallel-sided platform tapering abruptly at the anterior end. Specimens from Innerkip and the Teeswater River localities have shorter, more gradually tapering plat- forms with fewer denticles. These differences probably reflect geographic variations. Biostratigraphy Distribution of the conodont faunas appears to be governed by environmental factors so that local biostratigraphic significance of the faunas is limited. However, further detailed sampling may substantiate distributional patterns that are here interpreted as poten- tially useful. For example, in the Niagara Peninsula few samples of the Bois Blanc Formation contain "advanced" forms of Icriodus latericrescens robustus, while they are abundant in the overlying Edgecliff Member. Farther west (Innerkip, Teeswater River) the "advanced" forms are common in the Bois Blanc. At Innerkip in particular the "advanced" forms are common in the basal bed of the formation. If the occurrences in the Niagara Peninsula are an accurate repre- sentation of the fauna, then the Bois Blanc is a markedly diachronous rock unit. Also, the distribution of /. latericrescens robustus could be used to define the Bois Blanc in the Niag- ara Peninsula, particularly where only sub- surface material is available and diagnostic lithological characteristics cannot be exam- ined. We believe that the irregularities in distri- bution of the simple cones are attributable to environmental factors. Except in one sam- ple, T503 from locality 2, the Coelocerodon- tus sp.- Pa nderodus valgus group is rare in the Bois Blanc Formation. Further sampling is required to determine if this restriction is constant. Orr (1971) proposed a biostratigraphic zo- nation using conodont faunas of Early and Middle Devonian age of the Michigan Ba- sin. The conodont faunas from southern On- tario can be correlated with his Icriodus la- tericrescens robustus zone which ranges in age from late Early to early Middle Devoni- an. This, together with the probable diachro- nous nature of the Bois Blanc Formation, suggests that this is a lithostratigraphic unit that may transgress the Lower-Middle De- vonian boundary. Direct intercontinental correlation is im- possible not only because of the low diver- sity of the conodont faunas, but more importantly because of the complete absence of platform elements other than Icriodus la- tericrescens robustus and very rare specimens of Spathognathodus. I. latericrescens robustus is not known from outside eastern North America. Palaeoecology The possible environmental effect on distri- bution of the conodonts from the Niagara Peninsula was tested by grouping the sam- ples according to abundance of icriodiform elements versus abundance of simple cones (excluding Acodina). Three groups were es- tablished: a) samples containing a markedly higher proportion of icriodids; b) samples containing a markedly higher proportion of simple cones; c) samples in which the numbers of both types are approximately equal. Generally, the first two groups correspond to particular lithologies or depositional envi- ronments, and it is possible to speculate upon the controlling factors of the conodont distribution. Most samples from the Bois Blanc For- mation contain a higher proportion of icriodids than of simple cones. The Bois Blanc is a thin, transgressive limestone unit, presumably representing relatively high en- ergy, shallow water, nearshore conditions. The limestones are laminated, thinly or ir- regularly bedded, and contain abundant chert (as nodules or thin beds) and varying amounts of terrigenous clastic material. The lower metre of the formation is often com- posed of glauconitic quartz sandstone. The megafauna includes brachiopods, trilobites, crinoids, corals, and gastropods (Oliver, 1967). During deposition of the formation factors such as rate of sedimentation, supply of terrigenous sediments, wave and current action, and salinity would have been varia- ble. The greater proportion of icriodids in the Bois Blanc may be due to either a prefer- ence or tolerance for such variable and seemingly stringent conditions, or may be the result of sorting by high energy processes that caused the more delicate simple cones to be broken up and removed. Simple cones form the greatest proportion of the conodont faunas in biostromal and biohermal facies of the Edgecliff Member. These facies contain richly fossiliferous (mainly corals and crinoids), cherty, bioclas- tic limestones which lack the terrigenous clastic component exhibited by the underly- ing Bois Blanc. Shallow water conditions again are indicated but the more uniform bedding, composition, and megafauna sug- gest a more stable environment than was present during deposition of the Bois Blanc. Small coralline patch reefs and coral-crinoid mounds up to 100 metres in diameter are common (Telford and Tarrant, 1975b). Within the mounds and close to or within the reefs, simple cones are 25 to 50 times more abundant than are icriodids. Sample T505 (Table 2) was taken from a small coral mound and demonstrates the dominance of simple cones in this lithology. Away from the reefs and mounds, in more regularly bed- ded though still richly coralline biostromal limestones, icriodids are abundant. Difference in water depth may be one of several factors involved in producing this distribution pattern, i.e., conodontophorids bearing only simple cones inhabited the shoal areas while those bearing icriodids flourished only in slightly deeper water be- tween the reefs and mounds. This interpreta- tion generally corresponds to the conodont palaeoecological models of Seddon and Sweet (1971) and Druce (1973) which are based primarily on depth stratification of co- nodont faunas. Druce (1973) described a se- ries of biofacies, representing shallow to deeper water environments, that are charac- terized by particular conodont taxa or com- binations of taxa. His shallowest water facies (Biofacies i) of the Lower Devonian contains only simple cones. Biofacies n (slightly deeper water) also contains some simple cones but is typified by the abundance of platform conodonts such as Icriodus. The Edgecliff Member of the Niagara Peninsula therefore contains conodonts of both Biofacies I and n; however, Biofacies I is uncommon and seems to be dependent on the presence of reefs and biohermal mounds, thus indicating that environmental factors additional to water depth exerted strong controls over conodont distributions. The specialized nature of the reef environment and the differences in nutrient supply, wave energy, and substratum character between reef and inter-reef areas were probably more effective in separating the conodont biofa- cies than water depth. Actually, the differ- ences in water depth during deposition of dif- ferent lithofacies of the Edgecliff Member were small, as indicated by the less than 10 metres of relief exhibited by the biohermal and reefoid structures (Telford and Tarrant, 1975b). Absence of Polygnathus Species of Polygnathus are well represented in upper Lower Devonian sequences of Eu- rope (Ziegler, 1971), western North America (Klapper et al., 1971), and eastern Australia (Telford, 1975), and they form the basis for intercontinental correlation between strati- graphic units of these regions. It is unusual for Polygnathus to be absent as is the case in strata of Early Devonian age in the Appa- lachian and Michigan basins (Klapper et al., 1971). Polygnathids are normally abundant in Middle Devonian marine strata but they are absent from the lower Middle Devonian Edgecliff Member of New York State (Klap- per et al., 1971) and Ontario (this study). In the central New York portion of the Appalachian Basin polygnathids make their first appearance in the Nedrow Member of the Onondaga Formation (Klapper, 1971). In the Niagara Peninsula of Ontario, strata determined to be lithostratigraphically equivalent (Oliver, 1967) to the Nedrow Member (upper Edgecliff and Clarence members of Telford and Tarrant, 1975b) have icriodids as the sole platform elements. The relatively late appearance of polygnath- ids in the Appalachian Basin is possibly the result of major palaeogeographic barriers. However, the difference in occurrence of po- lygnathids between central New York and Ontario can also be attributed to local envi- ronmental controls. The Nedrow Member consists mainly of thin-bedded, argillaceous limestone (Oliver, 1954) that represents deeper water, nonreef deposition, and more stable conditions than do the biostromal or biohermal limestones of other members of the Onondaga Formation. Davis (1975) noted a similarly controlled distribution of icriodid and polygnathid conodonts in the upper Middle Devonian Tully Limestone of central New York. Acknowledgments We are grateful to Miss Joan Burke for typ- ing the manuscript and to Mr. Huibert Sa- belis for drafting Figures 2 and 3. 10 Appendix Locality information and stratigraphic de- scriptions of localities 1 to 9. Sample codes are indicated after measurements (e.g., 202, 202A, etc.) LOCALITY 1 Quarry (north face) of George C. Campbell Company Limited. Lot 8, cone, vm, Bertie Township. 0-10.2 metres, Bertie Formation; 10.2-12.1 metres, Bois Blanc Formation. 0-3.8 m: medium bedded, brown dolo- stone with bituminous lamina- tions. 3.8-6.5 medium bedded, grey, argilla- ceous dolostone. 6.5-8.0 thin or irregularly bedded, grey- brown, finely crystalline dolo- stone. 8.0-10.2 thin or irregularly bedded, mot- tled grey and cream, very finely crystalline dolostone. 10.2-10.3 grey shale. 10.3-12.1 medium bedded, cherty, very fossiliferous, bioclastic lime- stone; conodont samples at 10.3-10.5 (201, 2601) and 11.8-12.1(202, 202A). LOCALITY 2 Quarry (east face) of Ridgemount Quarries Limited. Lot 3, cone, vm, Bertie Township. 0-4.6 metres, Bertie Formation; 4.6-8.2 me- tres, Bois Blanc Formation; 8.2-16.6 metres, Edgecliff Member of Onondaga Formation. 0-4.6 m: thin or irregularly bedded, mot- tled grey-brown and cream, very finely crystalline dolostone. 4.6-4.9 greenish, glauconitic sandstone. 4.9-5.1 grey shale. 5.1-8.2 irregularly bedded, cherty, fossil- iferous, partly argillaceous lime- stone; conodont sample at 5.2-5.4(301). 8.2-8.9 coarse-grained, crinoidal bioclas- tic limestone; conodont samples at 8.2-8.3 (302) and 8.6-8.9 (501). 8.9-16.6 irregularly bedded, cherty, coral- line bioclastic limestone; cono- dont sample at 1 1.1-13.2 (303). LOCALITY 3 Abandoned quarry (northwest and south- west faces). Lot 6, cone. I, Wainfleet Township. Northwest face: 0-7.4 metres, Edgecliff Member of Onondaga Formation. 0-2.9 m: medium bedded, dark grey to black, very fossiliferous, argilla- ceous limestone; conodont sam- ples at 0.6-1.8 (901) and 2.8-2.9 (9101). 2.9-4.3 massive, coralline limestone. 4.3-7.4 medium bedded, cherty, very fossiliferous, coral-crinoid bio- clastic limestone; conodont sam- ples at 4.3-4.5 (9102), 5.8-6.7 (902), and 7.1-7.4 (9103). Southwest face: 0-7.5 metres, Edgecliff Mem- ber of Onondaga Formation. 0-1.2 m: medium bedded, dark grey to black, very fossiliferous, argilla- ceous limestone; conodont sam- ple at 0.9-1.2 (1001). 1.2-2.4 medium bedded, crinoidal bio- clastic limestone; conodont sam- ple at 1.8-2.0(1002). 2.4-2.9 medium bedded, brown lime- stone with shale partings; cono- dont sample at 2.6-2.8 (1003). 2.9-3.2 grey-brown, uniformly textured, crinoidal bioclastic limestone; conodont sample at 3.1-3.2 (1004). 3.2-7.5 medium bedded, cherty, very fossiliferous, coral-crinoid bio- clastic limestone; conodont sam- ples at 3.4-3.5 (1005) and 7.4-7.5 (9104). LOCALITY 4 Quarry (northwest face) of Cayuga Materials and Construction Company Limited. Lots 45 and 46, cone. I North, North Cayuga 11 Township. 0-8.8 metres, Bertie Formation; 8.8-11.8 metres, Oriskany Formation; 1 1.8-13.7 metres, Bois Blanc Formation. 0-1.2 m: thin to medium bedded, grey, ar- gillaceous dolostone. 1.2-3.5 thin to medium bedded, brown and grey mottled, very finely crystalline dolostone. 3.5-8.8 medium bedded, brown, uni- formly textured dolostone with biuminous laminations. 8.8-11.8 massive, grey-white, medium to coarse grained, quartzose sand- stone. 11.8-13.7 irregularly bedded, brown to light brown, cherty, weakly fos- siliferous, sandy limestone; co- nodont sample at 12.3-13.2 (2001). LOCALITY 5 Abandoned quarry (east face). Lots 13 and 14, cone, xili, Walpole Township. 0-0.5 me- tres, Bertie Formation; 0.5-2.9 metres, Bois Blanc Formation; 2.9-6.1 metres, Edgecliff Member of Onondaga Formation. 0-0.6 m: medium bedded, brown, uni- formly textured dolostone. 0.6-2.9 irregularly bedded, cherty, very fossiliferous bioclastic limestone with abundant shale partings; conodont samples at 0.8-1.1 (41) and 2.8-2.9 (2901). 2.9^4.7 medium bedded, noncherty, cri- noidal bioclastic limestone; co- nodont samples at 2.9-3.1 (2902) and 4.5^.7 (2903). 4.7-6.1 medium to thin bedded, cherty, very fossiliferous, coralline lime- stone; conodont samples at 4.7^.9 (2904), 4.7-6.1 (42), and 5.8-6.1 (43). LOCALITY 6 Quarry (west face) of R.E. Law Crushed Stone Limited. Lot 5, cone, n, Humberstone Township. 0-2.2 metres, Bertie Formation; 2.2-6.6 metres, Bois Blanc Formation; 6.6-11.0 metres, Edgecliff Member of Onon- daga Formation. 0-2.2 m: thin or irregularly bedded, mot- tled grey and cream, very finely crystalline dolostone. 2.2-2.3 grey shale. 2.3-2.9 dark brown, cherty, calcareous sandstone; conodont sample at 2.3-2.9(9001). 2.9-3.5 medium bedded, grey-green, glauconitic sandstone; conodont sample at 2.9-3.5 (9002). 3.5-5.9 interbedded sandstone and bio- clastic limestone with chert no- dules; conodont samples at 4.7-5.0 (9003) and 5.6-5.9 (9004). 5.9-6.6 dark brown, cherty limestone with shale partings; conodont sample at 5.9-6.5 (9005). 6.6-8.1 medium bedded, dark grey- brown, noncherty, fossiliferous, argillaceous limestone; conodont sample at 6.6-6.9 (9006). 8.1-9.3 medium bedded, weakly cherty, very fossiliferous limestone with shale partings; conodont sam- ples at 8.1-8.3 (9007) and 8.9-9.3 (9008). 9.3-11.0 irregularly bedded, dark brown, cherty, coralline limestone; co- nodont sample at 9.8-10.2 (9009). LOCALITY 7 Abandoned quarry (west face), Innerkip. Lot 9, cone, xvn. East Zorra Township. 0-0.9 metres, Bass Islands Formation, 0.9-5.6 metres, Bois Blanc Formation. 0-0.9 m: medium bedded, brown, very finely crystalline, weakly lami- nated dolostone. 0.9-5.6 irregularly bedded, grey-brown, cherty, fossiliferous limestone with shale partings; conodont sample at 0.9-1.5 (9201). LOCALITY 8 East side of Teeswater River at Pinkerton, about 40 km north of Wingham. Bois Blanc Formation. 12 0-1.2 m: irregularly bedded, cherty, fossil- iferous sandy limestone; cono- dont sample at 0.6-0.9 (9401 ). LOCALITY 9 East side of Teeswater River, 1.5 km south- west of Cargill, about 32 km north of Wingham. Bois Blanc Formation. 0-0.5 m: cherty, fossiliferous, sandy lime- stone; conodont sample at 0-0.5 (9501). Literature Cited BEST. E.W. 1953 BULTYNCK. P. 1971 Pre-Hamilton Devonian stratigraphy, southwestern Ontario, Canada. -Ph.D. thesis. University of Wisconsin. 209 pp. Le Silunen Supeneur et le Devonien In- ferieur de la Sierra de Guadarrama (Es- pagne Centrale). Deuxieme partie: As- semblages de Conodontes a Spathognathodus. -Bulletin, Institut Royal des Sciences Naturelles de Belgique, 47(3): 1-43. DAVIS. WE, JR 1975 Significance of conodont distribution in the Tully Limestone (Devonian), New York State. -Journal of Paleontology, 49(6): 1097-1104. DRUCE. EC. 1973 Upper Paleozoic and Triassic conodont distribution and -the recognition of biofacies. In Rhodes, F.H.T., ed. Cono- dont paleozoology. -The Geological Soci- ety of America Special Paper, 141: 191-237. HEWITT. D.F 1972 KLAPPER. G. 197' Paleozoic geology of southern Ontario. -Ontario Division of Mines, Geological Report, 105: 1-18. Sequence within the conodont genus Polygnathus in the New York Lower Mid- dle Devonian. -Geologica et Palaeontolo- gica, 1: 59-79. KLAPPER. G AND G.M. PHILIP 1972 Familial classification of reconstructed Devonian conodont apparatuses. -Geologica et Palaeontologica, SB 1 : 97-114. KLAPPER. G .. C.A SANDBERG. C COLLINSON. J.W. HUDDLE. R WILLIAM ORR, L.V. RICKARD. D. SCHUMACHER. G. SED- DON ANDT.T. UYENO 1971 North American Devonian conodont biostratigraphy. -Symposium on cono- dont biostratigraphy, Geological Society of America Memoir, 127: 285-316. KLAPPER. G AND W Z1EGLER 1967 Evolutionary development of the Icriodus latericrescens group (Conodonta) in the Devonian of Europe and North America. -Palaeontographica, Abt. A, 127: 68-83. OLIVER, W A . JR 1954 1967 ORR. R W 1971 Stratigraphy of the Onondaga Limestone (Devonian) in central New York. -Bulletin of the Geological Society of America, 65: 621-652. Stratigraphy of the Bois Blanc Formation in New York. -United States Geological Survey Professional Paper, 584A. 8 pp. Conodonts from Middle Devonian strata of the Michigan Basin. -State of Indiana Department of Natural Resources, Geo- logical Survey Bulletin, 45: 1-1 10. SANFORD, B V 1969 Geology of the Toronto-Windsor area, Ontario. -Geological Survey of Canada, Map 1263A. SEDDON, G AND W C. SWEET 1971 An ecologic model for conodonts. -Journal of Paleontology, 45(5): 869-880. TARRANT, G A. 1975 Lower and Middle Devonian conodonts from Stevensville, Ontario. -B.Sc. thesis. University of Waterloo. 62 pp. 13 TELFORD, P.G. 1975 Lower and Middle Devonian conodonts from the Broken River Embayment, North Queensland, Australia. -Palaeontology, Special Paper 15: 1-96. TELFORD. PC AND G.A. TARRANT 1975a Paleozoic geology of the Dunnville Area, southern Ontario. -Ontario Division of Mines, Preliminary Map P. 988, Geologi- cal Series. 1975b Paleozoic geology of the Welland-Fort Erie area, southern Ontario. -Ontario Di- vision of Mines, Preliminary Map P. 989, Geological Series. VON BITTER. PH. 1972 Environmental control of conodont distri- 1976 ZIEGLER. W 1971 button in the Shawnee Group (Upper Pennsylvanian) of eastern Kansas. -University of Kansas Paleontological Contributions, Article 59: 1-105. The apparatus of Gondolella sublanceolata Gunnell (Conodontophonda, Upper Pennsylvanian) and its relationship to Illi- nella typica Rhodes. -Life Science Contri- bution, Royal Ontario Museum, 109: 1^*6. Conodont stratigraphy of the European Devonian. -Symposium on conodont biostratigraphy. Geological Society of America Memoir, 127: 285-316. 14 Suggested citation: Life Sci. Occ. Pap.. R. Ont. Mus. All manuscripts considered for publication are subject to the scrutiny and editorial policies of the Life Sciences Edi- torial Board and to review by persons other than Museum staff who are authorities in the particular field involved. Price: $1.00 <■ The Royal Ontario Museum, 1977 100 Queen's Park, Toronto. Canada M5S 2C6 PRINTED IN CANADA BY HUNTER ROSE ISBN 0-88854-198-8 ISSN 0082-5107 16 *v/fcs, n^y ^^9/7° 7*