MARCH 5, 1996 Begun in 1895 | YOLUME 109, NUMBER 349 | Stromatoporoids from the Emsian (Lower Devonian) of Arctic Canada by Eric Prosh and Colin W. Stearn Paleontological Research Institution 1259 Trumansburg Road Ithaca, New York, 14850 U.S.A. .. PALEONTOLOGICAL RESEARCH INSTITUTION Officers PRESIDENT naaa و‎ ETT DOS a TAE SE VA A JOHN C. STEINMETZ NIGER PRESIDENT ᷑ d;!!! EE RICHARD E. PETIT SERRARA ee EE HENRY W. THEISEN J NS VO v ed pee AC TT PAMELA WAIT DIRECIORE ei o fd ل كت و ا‎ WARREN D. ALLMON Trustees R. TUCKER ABBOTT (to 6/30/96) RICHARD E. PETIT (to 6/30/96) Bruce M. BELL (to 6/30/96) EDWARD B. Picou (to 6/30/98) CARLTON E. BRETT (to 6/30/98) GARY ROSENBERG (to 6/30/96) WILLIAM L. CREPET (to 6/30/97) CONSTANCE M. SOJA (to 6/30/97) J. THOMAS DuTRO, JR. (to 6/30/96) JAMES E. SORAUF (to 6/30/97) SHIRLEY K. EGAN (to 6/30/98) JOHN C. STEINMETZ (to 6/30/97) ANTON J. EGNER (to 6/30/97) SUSAN B. STEPHENS (to 6/30/96) M. G. HARASEWYCH (to 6/30/98) HENRY W. 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Numbers of Palaeontographica Americana are priced individually, and are invoiced separately on request. for additional information, write or call: Paleontological Research Institution 1259 Trumansburg Road Ithaca, NY 14850 USA (607) 273-6623 FAX (607) 273-6620 @ This paper meets the requirements of ANSI/NISO 239.48-1992 (Permanence of Paper). MARCH 5, 1996 Begun in 1895 ۲ QO« Á ) YOLUME 109, NUMBER 349 Stromatoporoids from the | Emsian (Lower Devonian) of Arctic Canada by | Eric Prosh and Colin W. Stearn Paleontological Research Institution 1259 Trumansburg Road Ithaca, New York, 14850 U.S.A. ISSN 0007-5779 ISBN 0-87710-440-9 Library of Congress Catalog Card Number: 95-071054 | Printed in the United States of America Allen Press, Inc. | Lawrence, KS 66044 U.S.A. CONTENTS | Page ) .. ⅛ Up“ 5 E a a s AI 5 Ali DOOR M RM a ñ ñ⁊ñ ß ß 5 Stratigraphy MAURO pa عت‎ a oe وى موك‎ e d | EE 6 | ONE 6 | , dd !...... 6 | USSK OTO den e ñðßygd I 9 | FCC / ↄ VVV. / . 9 npani taoca ukuni nka BBA SAA AA tec cr er T EE 9 Conodont Biostratigraphy WE ینت‎ WO AA ZONES: fr WA eats ea A 9 VEU LON E AAA A AA 10 reis ee e ß 10 EC Zones c o. ner 10 Stromatoporoid Biostratigraphy and Paleogeography Southwestern Ontario and North-Central Un SU U 11 tan (EE ĩ v 1i Ri 11 EE ecc dd 13 Systematic Paleontology E heres OP tee 77). mU Hau ی وق‎ ee 13 Systematics Order Actinostromatida Family Actinostromatidae | Genustacinostiona A AA a a EE 14 del P ß 15 NET EE EE 16 Order Clathrodictyida | Family Clathrodictyidae | Genus GM TON ان‎ OD E dd و‎ li éi | (SNS OSP ER TEOMA E I o e GE 19 A eer ñ mt TT 20 Family Tienodictyidae | UA iii 21 | ,! nn 22 | ed, RR 23 Order Stromatoporellida Family Stictostromatidae nne ęñę md EE 8 24 neh ß... o a 26 nee dd d Ls 27 Family Hermatostromatidae err d.. e 30 Order Stromatoporida Family Stromatoporidae , ⁵Mÿñꝶ q Ag 31 ian eienr ffn EE e 32 COSTS INDIO Ian aoa Pren KAA de AAA AA EE 33 Family Syringostomellidae ČISTE eino, o O ati EUN 34 بیس‎ 34 MOTUS IA ERA d Order Syringostromatida Family Syringostromatidae FF 35 hh EE . CONUS brot d U e SONGE 001516828 EE EE la Appendix Feen ůꝶ0 dd d Appendix 2. Catalogus-of Type Numbers and Locations s 8 e Ppendix 3. Collecting locations and stratigraphic posto), 8 = Elte E 8 be 46 e, DEE 64 | | LIST OF ILLUSTRATIONS Text-figure Page E nn وام ماله‎ OCIS IR Canadian ñỹꝶq CR X rre CU Y OR راح‎ Was Vey aio 1 2. Correlation chart of formations from which stromatoporoide were collectell..... 8 3, Stratigraphie ranges of Lower and lower Middle Devonian stromatoporolds, "ee SEENEN tre ham mee aor E sre ca 12 LIST OF TABLES Table Page 1. Comparativ . ²˙ of Srictostroma OFFENSE SS a STROMATOPOROIDS FROM THE EMSIAN (LOWER DEVONIAN) OF ARCTIC CANADA | ERIC C. PROSH AND COLIN W. STEARN | Earth and Planetary Sciences, McGill University, Montreal, Canada ABSTRACT Early Devonian limestones of Ellesmere, Bathurst, and smaller islands between them in the Canadian Arctic Archipelago contain a diverse fauna of stromatoporoid sponges. This fauna provides the best evidence in North America of the early recovery phase of this reef-building group from a diversity low at the Silurian/Devonian boundary, a recovery that lead to its diversity peak in Givetian time. Stromatoporoids from the lower member of the Blue Fiord Formation locally form large reefal masses. Well preserved stromatoporoids also occur less abundantly: 1. in the top of the underlying Eids Formation, 2. in the upper | member of the Blue Fiord Formation, 3. in the Disappointment Bay Formation, which is correlative of the upper Blue Fiord, | and, 4. in the overlying Bird Fiord Formation, and a correlative unnamed formation, both of which span the Lower/Middle Devonian boundary. The stratigraphic distribution of these stromatoporoids can be accurately determined according to conodont biostratigraphy as spanning the dehiscens to partitus (Emsian to basal Eifelian) conodont zones. Common occurrences of Stro- matoporella perannulata, Stictostroma gorriense, Habrostroma proxilaminatum, and Parallelopora campbelli in the arctic fauna and southern Ontario and the adjacent United States, indicate that the Detroit River Group is of similar Emsian age, and that the Eastern Americas realm was open to migration from the Arctic. Similarity of species with the Emsian faunas of Russia, | Australia and China suggests the cosmopolitan and eguatorial distribution of stromatoporoids in Emsian time and opens possibilities for using the group in correlation. The fauna is therefore important in establishing both the evolution of the order and also its geographic distribution in Early Devonian time. Twenty-five species (assigned to 22 genera) are described. The species concept used is a broad one and the range of variation in each taxon is documented. New species described are: Gerronostroma septentrionalis, Anostylostroma anfractum, Pseudoac- | tinodictyon conglutinatum, Stictostroma? nunavutense, Clathrocoilona vexata, Stromatopora hensoni. The morphologic limits of the following genera are considered in the description of species: Plectostroma, Aculatostroma and Atelodictyon, Clathrocoilona, | Salairella and Syringostromella. The range of Trupetostroma is extended downward into Emsian strata. | INTRODUCTION from the lower 100 m (lower Emsian, dehiscens Zone) of the Blue Fiord Formation in the type area between Eids and Sör Fiords (Text-fig. 1A). Of the 11 species described by Stearn (1983), eight are recognized in this study: Clathrodictyon ellesmerense Stearn, 1983, Ger- ronostroma septentrionalis n. sp., Clathrocoilona vex- ata n. sp., Stromatopora polaris, Stearn, 1983, Stro- matopora cf. S. hupschii (Bargatzky, 1881), Glyptos- tromoides simplex (Yang and Dong, 1979), Salairella prima Khromych, 1971, and Atopostroma distans (Ripper, 1937b). The three species that do not occur in the collections studied here, which were made by | Rocks of earliest Devonian age cover a relatively | small area of the North American platform because this was a time of worldwide regression at the close of | the Tippecanoe sequence. Reef faunas of this age are | restricted in their distribution and of low diversity. In North America the Kaskaskia transgression appears to | have started in the north and, spreading southward in | Shallow seas across the platform, brought with it a reef- building fauna rich in stromatoporoids. The first reef Complexes of regional extent built in this sea were in the area that is now the Canadian Arctic Archipelago i i i and are contained within the Blue Fiord Formation. Gary Smith and Eric Prosh, * all represented - | This study describes the elements of this resurgent reef Stearn's (1983) collections by single specimens. These | auna. In eastern and arctic North America the growth include Gerronostroma cf. G. immemoratum Bogo- Of the reef fauna in subsequent Middle and Late De- yavlenskaya, 1977, Amp hipora sp., and Labechia sp. | Vonian time was progressively inhibited by siliciclastic bi e e — — ene pea | 1 5 o ۰ s sii | DONI, but in the Western Canada Sedimentary ease bechia sp. has been tentatively identified as Syringo- | reefs thrived through the middle part of the period and : ; 1 1 A 1 - their growth culminated in giant Frasnian reef com- dictyon tuberculatum (Nicholson) by St. Jean ( 986) pl | exes, ACKNOWLEDGEMENTS We are grateful to Gary P. Smith who, in the prep- aration of his doctoral dissertation (Smith, 1984), col- This study expands and refines earlier work by Stearn | (1983) on the Emsian stromatoporoids of southern | Ellesmere Island. Stearn described a fauna collected | BULLETIN 349 unnamed limestone that has been referred to incor- rectly as the Blue Fiord Formation. Stromatoporoids were collected from this unnamed formation on Bath- urst Island by Smith and on nearby Truro Island by Prosh. EIDS FORMATION The Eids Formation (Text-fig. 2) consists mostly of calcareous siltstone and shale, with less limestone, silt- stone and sandstone. It conformably underlies the Blue Fiord Formation in southern and central Ellesmere Island (Trettin, 1978). West of Sör Fiord it reaches a thickness of 767 m (Uyeno, 1990). With the exception of the uppermost beds transitional to the Blue Fiord Formation, the Eids Formation is poorly fossiliferous. It ranges in age from Lochkovian to earliest Emsian. Silty carbonates on Bathurst and adjacent islands as- signed by Kerr (1974) to the Eids Formation are much younger than the Eids on Ellesmere Island. Stromatoporoid specimens identified in this study as from the Eids Formation come from the upper 100 m in the Blue and Sör fiords areas of Ellesmere Island. In these areas the upper Eids consists of dark gray, calcareous siltstone and mudstone with interbeds of fossiliferous lime wackestone and isolated bioherms (Smith, 1984). BLUE FIORD FORMATION The Blue Fiord Formation is an important and wide- ly distributed cliff-forming unit in the arctic islands. The best exposed sections occur on southern Ellesmere Island and adjacent islands. The type section was des- ignated by McLaren (1963) between Blue Fiord and Eids Fiord (Text-fig. 1A). The typical Blue Fiord is predominantly a dark fossiliferous limestone spanning most of the Emsian Stage (Smith, 1984). The Blue Fiord Formation has been recorded from the arctic islands west of Ellesmere Island (Thorsteins- son and Tozer, 1962) and from the subsurface (Mayr, 1980) in the Bent Horn oilfield (a short distance west of the northwest tip of Bathurst Island and just off Text- fig. 1C). Much of what has been referred to the Blue Fiord Formation in the western arctic islands, how- ever, is of Eifelian age, and should ultimately be re- ferred to a new, as yet undescribed formation (see un- named Formation below). Studies of Blue Fiord macrofossils include those of Brice (1982) and Jones and Boucot (1983) on brachio- pods, Ormiston (1967) on trilobites, and Pedder (1982, 1983) on corals. In the type area of the Blue Fiord Formation; McLaren (1963) recognized two members: a lower limestone and shale member and an upper brown lime” stone member. The lower member is about 700 m thick lected most of the specimens on which this study is based. The field work of Smith (in 1978, 1979, and 1980) and of Prosh (in 1983 and 1992) was made pos- sible by the logistic support of the Polar Continental Shelf Project of Natural Resources Canada. Smith’s field work was funded by Natural Resources Canada, the Natural Science and Engineering Council, and the McGill Centre for Northern Studies and Research. The research of Eric Prosh and Colin Stearn is funded by grants from the Natural Sciences and Engineering Re- search Council, Canada to Stearn. For critical com- ments that have improved the manuscript we are grate- ful to Barry Webby, Carl Stock, and Warren Allmon. STRATIGRAPHY INTRODUCTION The Emsian and basal Eifelian stromatoporoids de- scribed in this study were collected from the Eids, Blue Fiord, Disappointment Bay, Bird Fiord, and an un- named formation. The great majority of specimens were collected by Gary Smith and Colin Stearn from the Blue Fiord Formation (lower to upper Emsian) of Ellesmere Island. Most of the Blue Fiord specimens were collected along a broad outcrop belt extending from Blue and Bird fiords in the west to Sôr Fiord in the east (Text-fig. 1A). Because this outcrop belt in- cludes the type section of the Blue Fiord Formation, localities within the belt are referred to in the text as within the “type area” or in the “vicinity of the type section”. Supplementary collections from the Eids and Bird Fiord formations, which respectively underlie and overlie the Blue Fiord Formation (Text-fig. 2), were also included in the study. Collections of Smith and Stearn from the Blue Fiord Formation northeast of the type area in the vicinty of Vendom Fiord (Text-fig. 1B) and by Smith from southwestern Ellesmere Island at Muskox and Goose Fiords (Text-fig. 1C) were also studied. The location of the collections studied and the stratigraphic sections measured by Smith (1984) are plotted on Text-figure 1 and listed by latitude and lon- gitude in Appendix 1. The geology of this southern coast of Ellesmere Island has been described recently by Mayr et al. (1994). The Disappointment Bay Formation of Bathurst, Cornwallis, and adjacent islands is a correlative of the middle-to-upper Blue Fiord Formation of Ellesmere Island (Text-fig. 2). Small collections from the Dis- appointment Bay Formation on Truro Island (Text- fig. 1, loc. 34) made by Eric Prosh in 1983 and 1992 and from Lowther Island (Text-fig. 1, loc. 33) in 1983 are also described here. On Bathurst Island and neighbouring islands, the uppermost Emsian and Eifelian are represented by an N DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN Lee oi. Sör Fiord] Blue Fiord Bird Fiord A —J ELLESMERE E Goose, Fd, ISLAND RAN usko Ed CORNWALLIS 8 DEVON ISLAND 5 22 L ? > 5 E 18 办- Resolute | | 30 32 gerres B Text-figure 1.—Position of collecting localities in Canadian arctic islands. Precise positions by longitude and latitude for the numbered localities are given in Appendix 1. A. Blue Fiord-Sòr Fiord area. B. Vendom Fiord area. C. Localities outside A and B. The stippled boxes Show the positions of maps A and 13. Truro Island—34, Lowther Island—33. (689 m; Uyeno, 1990) and consists of brownish gray grainstone to packstone, coral-stromatoporoid bound- to brown nodular limestones and lesser interbedded stone. The upper brown limestone member is 572 m Bray calcareous mudstones and shales (McLaren, 1963). thick in a section near the type section (Uyeno, 1990) ; he lower member is cliff-forming, abundantly fossil- and consists of brown and brownish gray, bioclastic, lerous and contains large stromatoporoid-bearing coarse-grained limestone but contains relatively few bioherms. Smith (1984), and Smith and Stearn (1982, fossils. 19873) recognized a variety of lithologic units within On the west side of Vendom Fiord (Text-fig. 1B) the the lower member: interbedded lime mudstone and Blue Fiord Formation consists of about 1200 m of Shale, argillaceous fossiliferous wackestone, skeletal limestone and minor siltstone. Two informal units are BULLETIN 9 EE SOUTHERN BATHURST, TRURO, zones ELLESMERE ISLAND LOWTHER ISLANDS — Sr / — "ni partitus 0 ۰ unname {Ss è Al Bird Fiord Fm. formation 出 E patulus E serotinus Blue Fiord 2 ° Z Dolomitic Facies Disap p ointment < (Muskox & Goose Bay Fm. 72 inversus Fiords) 2 Blue LSI POPOL IO LOST TOD El gronbergi é Fiord Fm. dehiscens 2 — Eids Fm. 3 = Text-figure 2.—Correlation chart of formations from which stromatoporoids were collected. gan later than in the type area, in Late Emsian time (Text-fig. 2)(Mayr et al., 1994). This platformal dol- omitic facies also occurs on adjacent parts of Devon Island (Kerr, 1977; Prosh et al., 1988). Lithologically the dolomitic Blue Fiord consists of vuggy dolostone, vuggy lime mudstone, and dark fossiliferous lime wackestones and dolowackestones (Smith and Stearn, 1987b). The dolomitic Blue Fiord records a period of late Emsian transgression and platform inundation; it is approximately correlative with the upper member of the type Blue Fiord. Smith and Stearn (1987b) pro- posed that the dolomitic facies of the Blue Fiord be assigned to the Disappointment Bay Formation, but the term Blue Fiord is retained for these beds here (Prosh et al., 1988). recognized: 1) a lovver carbonate member about 900 m thick consisting of gray limestone with dolostone interbeds and dark grayish-brown limestone, and 2) an upper siltstone-carbonate member of greenish silt- stones, calcareous siltstones and limestone interbeds overlain by a resistant grayish-yellow limestone and dolostone (Uyeno, 1990). The upper siltstone-carbon- ate member is the same unit provisionally assigned to the Bird Fiord Formation by Jones (1982). To the north and east of the type area as far as central Ellesmere Island, Blue Fiord lithologies represent pro- gressively more restricted depositional environments (Kerr, 1976; Trettin, 1978). On southernmost Elles- mere Island at Goose Fiord and adjacent Muskox Fiord, the formation is mostly dolomitic and deposition be- easternmost end of Bathurst Island and at Dyke Ack- land Bay on the southern coast (Text-fig. 1C, locs. 35, 36). On the western coast of Truro Island (Text-fig. 1C, loc. 34) 4-6 m of the unnamed formation contain a coral-stromatoporoid biostrome locally up to 6 m thick. Stromatoporoids from this biostrome are in- cluded in this study. CONODONT BIOSTRATIGRAPHY In this study we have been able to relate the strati- graphic ranges of stromatoporoids directly to an es- tablished conodont zonation, in other words to the standard Emsian zonal scale (Text-fig. 2). This is in great measure due to the excellent work of Uyeno (1990) who has documented the conodont zonation of the Devonian of southern Ellesmere Island. Many of the stromatoporoids used in this study come from local- ities identical or closely comparable to those of Uyeno and Klapper (1980) and Uyeno (1990). In the following paragraphs, the biostratigraphic framework is outlined and the stratigraphic intervals bearing stromatopo- roids are placed in the standard conodont zonation. DEHISCENS AND GRONBERGI ZONES These zones comprise the lower Emsian. In a mea- sured section in the type area of the Blue Fiord For- mation, Uyeno and Klapper (1980) and Uyeno (1990) have recognized the dehiscens Zone in the lower 267 m of the lower member. The gronbergi Zone is rec- ognized by the first appearance of Polygnathus aff. P. perbonus as Polygnathus gronbergi itself does not oc- cur. In this section the gronbergi Zone is recognized in the 267 to 393 m interval of the lower member. Be- cause P. gronbergi is absent and the gronbergi Zone here spans a relatively small stratigraphic interval, we commonly combine the dehiscens and gronbergi zones in dating. Consequently, stromatoporoids occurring exclusively from the lower 250 m or so of the formation of the type area Blue Fiord are assigned to the dehiscens Zone. Stromatoporoids occurring through the lower member up to about 400 m are assigned to a combined dehiscens/gronbergi Zone. In the Vendom Fiord area, conodont zones in the lower member of the Blue Fiord Formation cannot be as precisely placed as in the type area (Uyeno, 1990). Conodonts and macrofossils associated with the de- hiscens Zone occur low in the formation. The dehiscens and gronbergi zones probably occur in the lower two thirds of the lower member here: P. inversus first ap- pears high in the lower member. Stromatoporoids from low in the lower member at Vendom Fiord are assigned to the dehiscens Zone; those from low to medial parts of the member to the combined dehiscens/gronbergi Zone. DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN BIRD FIORD FORMATION The Bird Fiord Formation overlies the Blue Fiord Formation conformably, and reflects in its lithology a transition to siliciclastic depositional conditions. It is widely distributed on southwestern Ellesmere Island, northwestern Devon Island and the Bathurst Island Sroup (Goodbody, 1989). It ranges in age from latest Emsian to Eifelian. In the type area on Ellesmere Island It is over 800 m thick (Goodbody, 1989). A few stromatoporoid specimens were studied from the lower Bird Fiord Formation in the type area on the north side of Bird Fiord. These beds (the Norwe- &an Bay Member of Goodbody, 1989) consist of bio- clastic sandy limestone and calcareous siltstone with minor shale and argillaceous siltstone. DISAPPOINTMENT BAY FORMATION This late Emsian formation (Text-fig. 2) has been Studied on Cornwallis Island, eastern Bathurst Island, and intervening smaller islands (Kerr, 1974; Thor- steinsson, 1980, 1986). It is mostly dolostone but lo- cally on Bathurst, Truro, and Lowther islands (Text- fig. 1C), rare limestones (low in the formation) are abundantly fossiliferous. ۱ On Truro Island, the Disappointment Bay Forma- tion consists mostly of light-colored, massive, vuggy, Microcrystalline dolostone with subordinate laminated dolostone. It is about 200 m thick (Kerr, 1974). On the northeastern tip near the base of the formation, Small reef knolls occur. Kerr (1974) and Thorsteinsson (1986) do not indicate this occurrence on their maps. Stromatoporoid specimens were collected from these Teef knolls of dark gray-brown, bituminous, fossilif- erous packstone. The small knolls are lithologically Similar to coeval larger knolls in the Disappointment Bay Formation on Lowther Island (Thorsteinsson, 1980; Prosh, 1989). UNNAMED FORMATION An unnamed unit consisting of limestone and minor dolostone and shale conformably overlies the Disap- Pointment Bay Formation on eastern Bathurst, Corn- Wallis, and intervening small islands (map unit D-1 of horsteinsson, 1986). On Bathurst Island it incorpo- rates most or all of what Kerr (1974) erroneously re- ferred to as the Blue Fiord Formation. Kerr’s Bathurst Island “Eids Formation”, a distal equivalent of his Blue Fiord Formation”, probably also belongs to the Unnamed formation (Thorsteinsson, pers. comm., 1592). The unnamed formation spans the Emsian-Ei- elian boundary and is 20-100 m thick (Thorsteinsson, 1986) (Text-fig. 2). Stromatoporoids used in this study were collected Tom the lower 100 m of the formation at the north- BULLETIN 349 gler and Klapper, 1985). Because in the arctic islands the nominal conodonts of neither of these zones has been recognized, this interval must be dated by other fossil occurrences and by stratigraphic context. For dating stromatoporoid occurrences, we treat this in- terval as the undifferentiated patulus Zone (i.e., com- bined patulus and partitus zones). Two formations that contain stromatoporoids span this interval: 1) the low- er Bird Fiord Formation of Ellesmere Island, and 2) the lower unnamed formation of Truro and eastern Bathurst Islands. 1) Uyeno (1990) placed the Lower-Middle Devo- nian boundary at or near the base of the Bird Fiord Formation at its type section. Although diagnostic con- odonts are absent, brachiopods and corals from higher in the formation suggest Eifelian and Dalejan (late Em- sian) ages (Uyeno, 1990). Goodbody (1989) considerd the basal Bird Fiord to be included in the patulus Zone. On this basis we date the stromatoporoids that have been collected from the lower Bird Fiord Formation on Ellesmere Island as coming from the undifferen- tiated patulus Zone. 2) Similar uncertainty in dating applies to the un- named formation of Truro and Bathurst islands. Kerr (1974) considered the lower unnamed formation (Blue Fiord of Kerr) as Eifelian and possibly latest Emsian in age, largely on the basis of its trilobite fauna. A sample of the unnamed formation analyzed for con- odonts by T. T. Uyeno yielded no specimens (Uyeno, pers. comm. 1993; GSC internal report 02-TTU-93). The age of the unit underlying the unnamed for- mation is important in estimating the age of the for- mation. In the area of Cornwallis, Truro and Lowther islands, the Disappointment Bay Formation is dated as inversus Zone (Thorsteinsson, 1980) on the basis of diagnostic conodonts recovered from rare limestones low in the formation. The upper Disappointment Bay Formation is assumed to span most, or all, of the ser- otinus Zone and the transition to limestones of the unnamed formation is assumed to begin at about the patulus Zone. This conclusion is based on correlation of the transition from Blue Fiord to Bird Fiord for- mations on Ellesmere Island with that between the Disappointment Bay and unamed formation in the Cornwallis Island area suggested by Thorsteinsson (1986). Stromatoporoids collected from the unnamed for- mation come from the base at Truro Island and from the lower 100 m of the formation on eastern Bathurst Island. In both areas they are probably of latest Emsian age (patulus Zone). Due to the uncertain dating of this interval, however, they are assigned to the undiffer- entiated patulus Zone. The stromatoporoid fauna offers some clue as to the In the Sôr Fiord area, Uyeno and Klapper (1980) have identified P. dehiscens from the uppermost beds of the Eids Formation. The full extent of its occurrence in this formation is not known, but presumably the base of the Emsian is near the top of the formation. Stromatoporoids from the highest beds of the Eids Formation are assigned to the dehiscens Zone; those 50 or more meters below the top of the Eids are pos- sibily uppermost Pragian. INVERSUS ZONE This zone is widely and readily recognized in arctic Devonian strata. In the Blue Fiord type area, the in- versus Zone spans the interval from 393 to 1104 m, the upper half of the lower member and much of the upper member (Uyeno, 1990). At Vendom Fiord the inversus Zone ranges from the upper part of the lower member through much of the upper member of the Blue Fiord Formation. In both the type and Vendom Fiord areas, in the upper member. of the formation, stromatoporoids are relatively rare and are assigned to a combined inversus/serotinus Zone. On southernmost Ellesmere Island, the dolomitic facies of the Blue Fiord Formation ranges in age from the inversus to serotinus zones (Smith and Stearn, 1987b). Stromatoporoids from this dolomitic facies from Muskox Fiord and Goose Fiord areas, are all from low in the formation and assignable to the in- versus Zone. Although the lower Disappointment Bay Formation is firmly dated as inversus Zone, the upper part is dol- omitic and evaporitic and unfossiliferous. Stratigraph- ic relations suggest that the formation spans the full serotinus Zone as well. Stromatoporoids from the lower Disappointment Bay Formation at Truro and Lowther islands occur within the inversus Zone (Thorsteinsson, 1980). SEROTINUS ZONE In a section 2.5 km east of the type section of the Blue Fiord Formation the serotinus Zone is identified in the interval of the upper member from 1104 m to the top of the formation at about 1260 m (Uyeno, 1990). At Vendom Fiord the zone is recognized in the uppermost part of the Blue Fiord upper member. Al- though P. serotinus itself ranges up into the overlying Bird Fiord Formation, the overall faunal and strati- graphic context suggests that the zone ends at the top of the Blue Fiord Formation in the type area (Uyeno, 1990). UNDIFFERENTIATED PATULUS ZONE The Emsian-Eifelian boundary is placed at the boundary between the patulus and partitus zones (Zie- DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 11 Oliver and Pedder, 1989) and on stromatoporoids (Stock, 1990) was not as absolute as proposed, has already been suggested by Stearn (1983) and is fully supported by this study. The migration route of stro- matoporoids across the present site of Hudson Bay may have been closed to rugose corals by ecological barriers. Evidence is accumulating that environments favorable to stromatoporoids and tabulate corals may have been different from those that favored rugose corals (Mallamo et al., 1993). In any case, the paleo- geographic reconstructions of Oliver (1976b), Oliver and Pedder (1989), and Witzke (1990) need to be mod- ified to show an open seaway connection between the Arctic Islands and southwestern Ontario. NORTHERN ASIA Plectostroma salairicum (Yavorsky) is known in the Arctic from the unnamed formation (Bathurst Island) and from the Kuznetsk Basin of central Russia (Ya- vorsky, 1930). The age of both these occurrences is virtually identical, at or near the Emsian-Eifelian boundary. Aculatostroma cf. A. kaljanum (Bogoyav- lenskaya) from the lower Emsian part of the Blue Fiord Formation is known (as Coenellostroma kaljanum Bo- goyavlenskaya) from the eastern slope of the northern Urals and from lower Emsian strata (Bogoyavlenskaya, 1977; Khodalevich et al., 1982). Gerronostroma cf. G. immemoratum Bogoyavlenskaya, described by Stearn (1983) from the lower Blue Fiord, also was originally described from this fauna. Atelodictyon cf. A. solidum Khromych (Blue Fiord Formation, inversus Zone) was previously recorded (4. cylindricum solidum Khro- mych) from probable mid-to-late Emsian rocks in northeastern Siberia (Khromych, 1971, 1976). Two other arctic species are also recorded from Russia, but appear to be longer ranging. Syringostromella zintch- enkovi Khalfina occurs in the upper Lochkovian of the Salair, southcentral Russia (Khalfina, 1961) and Sa- lairella prima Khromych from probable Pragian rocks in Severo-Vostok, eastern Siberia (Khromych, 1971, 1976). Both of these species also occur in Australia (see below). AUSTRALIA AND CHINA Affinities with the Early Devonian faunas of Victoria (Webby et al., 1993) are indicated by the cosmopolitan species Syringostromella zintchenkovi Khalfina, Stro- matopora polaris Stearn, Atopostroma distans (Ripper) and Salairella prima Khromych. The arctic Emsian fauna shares 7 genera in common with the 11 taxa described by Webby and Zhen (1993) from the Jesse Limestone of New South Wales. At the specific level Atopostroma distans and Salairella prima occur in both faunas. age of the lower unnamed formation (Text-fig. 3). Some faunal turnover is apparent between the the Blue Fiord (dehiscens to serotinus zones) and the unnamed for- mation (undifferentiated patulus Zone) collections, but a significant number of species range through both as- Semblages. This suggests that no hiatus separates the Blue Fiord and younger assemblages. STROMATOPOROID BIOSTRATIGRAPHY AND PALEOGEOGRAPHY E In this study stromatoporoid ranges have been pre- Cisely dated, allowing meaningful comparisons of the arctic Emsian fauna to coeval faunas world-wide and the assessment of the biostratigraphic usefulness of Stromatoporoids (Text-fig. 3). Of the 25 taxa described In this study, 13 have been recorded from other places and supply information on the distribution of stro- Matoporoid faunas in Emsian time. These regions are, In decreasing order of similarity and importance: 1) north-central United States and southwestern Ontario, 2) Russian Asia, 3) southeastern Australia, and 4) Chi- na. When localities sharing species with the Arctic Em- Stan fauna are plotted on a reconstruction of the con- ünental configurations of Early Devonian time, such as that of Scotese (Stock, 1990), they are distributed throughout the tropical world of that time. On a broad Scale the Emsian stromatoporoid fauna appears to have been a cosmopolitan one and stromatoporoids must E" propagated along the tropics with little impedi- ent, SOUTHWESTERN ONTARIO AND NORTH-CENTRAL UNITED STATES Four species known only from this mid-continent region, Stromatoporella perannulata Galloway and St. Jean, Stictostroma gorriense Stearn (=mamilliferum Galloway and St. Jean), Habrostroma proxilaminatum Fagerstrom), and Parallelopora campbelli Galloway and St. Jean, have been identified in the arctic Emsian fauna. In addition the arctic Trupetostroma sp. and P Seudoactinodictyon conglutinatum n. sp. are closely Comparable to species from southwestern Ontario (Fa- 8erstrom, 1982). This sharing of species has led Prosh and Stearn (1993) to conclude that the Detroit River Toup of southern Ontario is entirely of Emsian age. * reasoning that led to the reinterpretation of the Correlation of the Detroit River Group is presented elsewhere (Prosh and Stearn, 1993). The identity of SPecies indicates a dispersal of stromatoporoids along an open seaway connection from the Arctic to the mid- Continent during serotinus Zone time and perhaps as “arly as during inversus Zone time. That the isolation of the Eastern Americas Realm of Oliver (1976b) based On the distribution of rugose corals (Oliver, 1976a; Text-figure 3.—Stratigraphic ranges of Lower and lower Middle Devonian stromatoporoids. dehiscens Inversus serotinus gronbergi NVISINH patulus BULLETIN 349 1112001/22 VLOdOJI DAVAJ UNIDUNUDIXOAd DUOLISOUQOH SUDISIP ۴ 121/7 #7 5 14021/21012 6 xajduns 52۳1010۸50 10yruuoďniy , Jo 11101152127 11/250711 "S [122 9 1uosuau VAOdOJDUOJLJE S11D]Od 4 ‘ds 01101201147 171101240 01/01102012 ASUAINADUNU 6 284214408 1 1711111/12 6 5 ۹ 9 unmuumnòduoo 0 11/111210! 117 ۴ 11121105 ^y ۰12 0217 | ds 12 5112101411021025 DUOLISOUOLLIN) 251/21211152112 1021۳00411909 mms / "jo DWUOHSOWMIY UNIILIO[OS 03 y ds ۳ costatus partitus NVI 1 12 DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 13 (e.g., Fagerstrom, 1982), and a much broader concept of the stromatoporoid species has ensued. The species concept we apply here is a relatively broad one (Stearn, 1989a). Many stromatoporoid species demonstrate signifi- cant structural or morphometric variability. In many species a large proportion of the range of variability may be expressed within a single skeleton. In general, a grouping of specimens may be confidently considered a unique species when the range of variability (however broad) is continuously expressed across the full col- lection, with no major gaps or discontinuities. An ob- vious precondition for recognizing the range of vari- ability is a relatively large number of specimens. A good indication of the broad species concept as applied herein is shown by a comparison of total species di- versity with generic diversity. The Arctic Emsian stro- matoporoid fauna comprises 25 species in 22 genera; only two genera are represented by more than a single species. A consequence of a broad species concept is that, in our opinion, the notion of subspecies is generally in- applicable to stromatoporoids. Because variability within a species is already great, rarely (if ever) will a given population consistently demonstrate character- istics deserving subspecies rank. Species synonymies listed are meant to be all-inclu- sive, listing all species considered identical to the spe- cies being described. Those species described as confere (cf) to an earlier description have the compared ref- erences listed in the synonymy (following cf.). Confere (cf) is the only nomenclatorial qualifier employed here. It is used for described species that closely resemble those described elsewhere. Reservation may be due to minor morphologic differences, too small a sampling to assure that the full range of variability is present, or inadequacies in the original description. Expanded study of such species may ultimately demonstrate that they are the named species (delete cf.) or, much less likely, that they are separate but closely related species. Species-level taxa are distinguished by letters (e.g., Actinostroma sp. A) when we judge that a distinctive morphology is exhibited that is likely to result in a new species being described when more and better speci- mens have been studied. If the material is sufficient for a generic identification only, the generic name is modified only by sp. (Trupetostroma sp. = a species of Trupetostroma). In the course of this study, approximately 800 thin- sections were examined. The preservation of identified specimens is graded according to the scale: exception- ally well preserved; well preserved; moderately well preserved; mediocre; poor. These categories are ap- proximate and subjective, but in general imply the The species Glyptostromoides simplex (Yang and Dong) is common to the Emsian of the south China continental plate and the arctic Emsian. DISCUSSION This synthesis demonstrates that the stromatopo- roids have more biostratigraphic value than has been Conventionally attributed to them. A prerequisite for the confident use of these fossils in correlation is that dating of occurrences be precise as in this study of the Emsian of the Arctic. Such dating has generally been lacking in classical studies of stromatoporoid system- atics in part because rigorous, internationally accepted Standards of dating postdate many of these studies. Stromatoporoids have been conventionally regarded as poor candidates for correlation in the belief that the Species are too long ranging and too provincial. Con- Servative taxonomic philosophies, species defined Without clear appraisal of range of variation within Skeletons or between specimens, and oversplitting of faxa have made recognition of species across national boundaries difficult. The recognition ofthe world-wide distribution and narrow stratigraphic range of some Species in this study demonstrates that the biostrati- graphic and paleogeographic value of this group is po- tentially great. Some genera in which taxonomic prob- lems at the species level persist, such as Stromatopora and Clathrocoilona, may be poor candidates for cor- relative purposes, but other genera, such as Stictostro- ma and Stromatoporella, where species are better de- fined, have great biostratigraphic potential. The chronologic development of stromatoporoids in arly Devonian time has recently been reviewed by Webby et al. (1993). The diversity and wide distri- bution of the Emsian world fauna shows that the rapid diversification of stromatoporoids to form the better- known reef complexes of Middle and Late Devonian lime was well underway in Early Devonian time. SYSTEMATIC PALEONTOLOGY INTRODUCTION à Stromatoporoids are an extinct class of sponges al- led to the extant coralline sponges (Stearn, 1972, 19753), Little can be gleaned from the distant stro- Matoporoid-sponge relationship, however, to assist in Setting limits to extinct stromatoporoid species. Most of the classical systematic studies of stromatoporoids (bre-1 960s) employed a species concept that by current Standards would be considered narrow. Sample suites Vere often limited in size and geographic scope, and 35 à result new species were plentiful. Many of these 3ve since been combined in synonymy. In more re- Cent years, larger samplings have been collected, and More attention has been paid to morphometric analysis ! | ۵ | | BULLETIN 349 digit number with the prefix GSC (e.g., GSC 108863). The locations from which these specimens were col- lected are listed in Appendix 2. The precise location of collections is recorded by latitude and longitude in Appendices 1 and 2 because very few geographic names are available in the High Arctic. Appendix 3 is a catalog of the other specimens identified in this study with their collection localities referenced to Appendix 1 and Text-figure 1. These specimens are in the general col- lections of the Geological Survey in Ottawa marked with a prefix number 110, 111, 120, or 129 followed by a hyphen and a second number (e.g., 110-286). The few types referred to by the prefix ROM are from the collection of the Royal Ontario Museum, Toronto, On- tario, Canada. SYSTEMATICS Class STROMA TOPOROIDEA Nicholson and Murie, 1878 Order ACTINOSTROMATIDA Bogoyavlenskaya, 1969 Family ACTINOSTROMATIDAE Nicholson, 1886 Genus ACTINOSTROMA Nicholson, 1886 Type species. — Actinostroma clathratum Nicholson, 1886. Actinostroma sp. A Plate 1, figures 1-3 Description. Skeleton large, hemispherical; surface bearing low mamelons closely and regularly spaced; no astrorhizae visible on surface. Vertical section: Laminae thin, flat or very gently undulate, consistently parallel, commonly passing lat- erally into a series of dots; thickness 0.02-0.04 mm, where poorly preserved may thicken to 0.06-0.08 mm, spaced 7 to 10 per 2 mm, average 8.3 (n=30). Lati- lamination absent, although successive spacing phases (vertical gradations of distantly to closely spaced lam- inae) 0.4—0.5 mm thick generally present. Pillars reg- ularly spaced, 9 to 10 per 2 mm, average 8.9 (n=30); thickness variable, 0.04—0.08 mm, average 0.06 (n=30); apparent vertical length limited, commonly span 1 to 5 laminae; maximum observed length 3 mm, long pil- lars generally slightly bent, rarely straight. ۴ uncommon, inconspicuous, defined by zones of gentle laminar doming, interlaminar dilation, and upward- divergent pillars; apparent vertical canal width 0.3-0.5 mm. Dissepiments scattered. Skeletal microstructure compact. Tangential section: In interlaminar areas, pillars form isolated dots, 0.04—0.06 mm diameter, a few joined by or bearing partial colliculi; towards and into laminar following. Exceptionally well preserved specimens pre- serve all macrostructure and especially microstructure in very fine detail, uniformly throughout the specimen; specimens of this quality are exceedingly rare. Well preserved specimens show little or no diagenetic al- teration; macrostructural details are fully preserved, and original microstructures are preserved over most of the specimen. Moderately well preserved specimens show some diagenetic alteration; macrostructure is largely unaffected, but microstructural detail may be obscured, although it is generally preserved at least locally. Most identified specimens are either well or moderately well preserved. Mediocre preservation ap- plies to specimens in which macrostructural details are obscured, at least partly, and no original microstruc- tural detail remains; specimens so preserved remain identifiable on macrostructural grounds only. Poorly preserved specimens preserve no microstructural de- tail, and macrostructures are largely obscured. In gen- eral, poorly preserved specimens cannot be confidently assigned (to species) in isolation, but can be identified in the context of the full collection studied. The value of classifying the preservation of speci- mens (in combination with the number of specimens identified) is that it allows the reader to gauge inde- pendently the confidence of the species identifications/ descriptions. This is particularly true for newly de- scribed species. Morphological measurements provided are in met- ric units, commonly centimetres (cm), millimetres (mm), or micrometres (um). Most measurements are derived from thin-section examination. Most fre- quently cited morphological parameters are laminar and pillar spacing, and laminar and pillar thickness. Laminar and pillar spacing are conventionally ex- pressed as number of laminae/pillars occurring per 2 mm distance, commonly cited as an average of n mea- surements with a minimum and maximum range of values per specimen or species. Morphological terminology follows the established literature on stromatoporoid systematics. Definitions of recently introduced terms may be found in such papers as Stearn, (1989b, 1991, 1993) and Stock (1989). Introductory glossaries appear in older papers such as Galloway and St. Jean (1957). In this report, we deviate from the normal terminology only for the following morphological feature. Where astrorhizae in tangential section are without walls and defined only by areas devoid of structural elements, the term “canal” or “tube” is inapproporiate; we use the term “astrorhizal path” or “path”. Type specimens designated in this report are housed in the Type Collection at the Geological Survey of Canada, Ottawa, Ontario, and are identified with a six- DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 15 Description. —Skeleton laminar to weakly domed, up to 10 cm diameter. Surface smooth; astrorhizae inconspicuous in hand-specimen. Vertical section: Dense network of pillars and sub- ordinate colliculate laminae. Pillars 0.03—0.05 mm thick; spaced 6 to 8 per mm, average 7.0 per mm (n=20, combined specimens); vertical extent variable 0.3-1.5 mm, commonly 0.5 mm; commonly thicker/ more opaque than colliculi; irregular thin phases of very dark pillars grossly resemble latilaminae, but true latilaminae absent. Colliculi thin 0.02-0.03 mm; com- monly arched (between neighbouring pillars), fewer straight/horizontal; dominantly arise at uniform levels to impart horizontal fabric to skeleton, locally network irregular; where colliculate laminae occur, spacing 7 to 9 per mm, commonly 7 to 8 per mm, specimen GSC 108853 average 7.8 range 7 to 9, GSC 108854 average 7.7 range 7 to 9 (each n=10). Skeletal microstructure compact. Astrorhizae prominent, vertically persistent; axial canal 0.20—0.30 mm diameter, canal walls 0.04— 0.05 mm thick; lateral canals branching downward from axial canal; astrorhizal tabulae (resembling enlarged colliculi) abundant, one for every three to five colli- culate laminae. Dissepiments absent. Tangential section: Pillars dark, solid dots 0.02—0.04 mm diameter; either isolated, or tightly linked by col- liculi into network; four, less commonly five, colliculi arise from each pillar. Astrorhizae simple, single axial canal surrounded by a few simple lateral canals, 0.12- 0.20 mm wide average 0.15 mm; center-to-center spac- ing 5 to 7 mm. Material.—Two specimens. Hypotypes GSC 108853, 108854. Well preserved. Discussion. —Yavorsky s (1930) original description and illustrations of Plectostroma salairicum closely match the Arctic specimens, and only a minor differ- ence in pillar spacing distinguishes the two (5 to 6 per mm for Yavorsky’s specimens, 6 to 8 per mm for those herein). The astrorhizal systems of the Arctic and Ya- vorsky’s specimens, however, are identical. Yavorsky (1930, p. 489) noted the locality of P. sa- lairicum as “Kuznetsk Basin, Kara-Chumysh River, in beds with Pentamerus pseudobaschkiricus Tschern." (now referred to Zdimir pseudobaschkiricus). The Zdi- mir pseudobaschkiricus—Megastrophia uralensis Zone includes mixed elements of both the patulus and par- titus Zones (conodonts), and is therefore uppermost Emsian and/or lowest Eifelian (Rzhonsnitskaya, 1988). This matches the age of the Bathurst Island unnamed formation, as currently understood (undifferentiated patulus Zone). Differences of opinion persist as to the assignment of species such as P. salairicum to the genera Plecto- stroma or Actinostroma. As noted by Nestor (1964, bands, pillars colliculate, forming polygonal network; Colliculi 0.01-0.02 mm thick. Preservation of colliculi Variable, poorly or unpreserved in much of specimen. Dissepiments log, arcuate lines joining several pillars. Astrorhizae small, ill-defined, indicated by vague paths of absent skeletal elements at and near mamelon sum- Mits; lateral path width approximately 0.2 mm. Material. — Large fragment of a single specimen ca. 40 cm basal diameter by 20 cm high. Hypotype GSC 108852. Well preserved. Discussion.—This specimen probably represents a New species of Actinostroma, but, despite locally ex- Cellent preservation, one specimen is insufficient ma- terial to establish the species. Since Fliigel’s (1959) monographic treatment of the genus Actinostroma, many species have been added, Still others removed to Plectostroma and Densastroma. Nonetheless, the basic species groupings recognized by Flügel (1959) remain valid. Of the three main Devo- Nan Actinostroma species-groups outlined by Flügel (4. clathratum, A. hebbornense, and A. stellatum spe- Cles-groups), this Arctic species shows closest affinity lo species of the 4. hebbornense group: thin laminae and pillars, both spaced about 5 per mm. Species from all three of these Devonian groups are most plentiful In the Givetian and Frasnian, but one Eifelian species, : Perspicuum Počta, 1894, shows interesting parallels to Actinostroma sp. A. Actinostroma perspicuum has Similar thin laminae and thin, relatively short pillars, but it is markedly cystose and has commonly conver- bent laminae. Although the Bohemian A. perspicuum (Choteč Limestone) and the Arctic specimen do not therefore appear to be closely related, both are char- acterized by very thin structural elements, primitive representatives of a general trend towards elemental thickening exhibited by later Givetian and Frasnian Species (Flügel, 1959). Occurrence. —Truro Island, unnamed limestone for- mation; highest Emsian/basal Eifelian (undifferentiat- 0؟‎ patulus Zone). Genus PLECTOSTROMA Nestor, 1964 PLECTOSTROMA SALAIRICUM (Yavorsky, 1930) Type species. — Actinostroma intertextum Nichol- Son, 1886. Plate 1, figures 4,5 Atinostroma salairicum Yavorsky, 1930, p. 489-490, pl. II, figs P ta. Es "dostroma salairicum (Yavorsky, 1930). Flügel and Flügel-Kahler, 8, p. 376 ? Aen? e Actinostroma salairicum Yavorsky. Khromych, 1984, p. 113-114, DI. VI, fig. 1. "mmm — — BULLETIN 349 Vertical section: Laminae colliculate, mostly contin- uous, very gently undulate; on a fine scale, ragged not smooth; locally inflected into shallow impersistent ma- melons; thin, 0.02-0.04 mm, commonly diagenetically thickened to 0.05—0.06 mm; spaced regularly, 8 to 11 per 2 mm, average 9.7 (n=10). Pillars short, confined to interlaminar interval, generally offset between suc- cessive laminae, rarely superposed; 0.04-0.06 mm thick, locally thickened to 0.08 mm; spaced regularly, 8 to 11 per 2 mm, average 9.4 (n=10). Colliculi arise sharply off pillars, forming vaulted cell-shaped galler- ies. Skeletal microstructure compact. Astrorhizae abundant, poorly formed; axial canals vertically im- persistent, roughly 0.6-0.8 mm diameter, many in- clined, may or may not be accompanied by impersis- tent mamelons; astrorhizal tabulae abundant, crowd- ed, thin 0.01-0.02 mm (but may be greatly thickened by diagenesis), dominantly sub-horizontal, flat or broadly convex, locally concave; lateral branches and tributaries indicated by lenticular or irregular zones of tabulae. Dissepiments (smaller than tabulae) in skeletal galleries, common not abundant. Latilaminae 3-4 mm thick, may be floored by thin band of sediment and thick (1-1.5 mm) basal layer of disordered skeletal material; thick root-like basal layer forms floor of spec- imen GSC 108855. Tangential section: Laminae diffuse meandering bands. Pillars vermiform or cateniform, locally linked into network: 0.04-0.06 mm thick; about one-quarter of pillars dot-like, 0.04-0.06 mm diameter; commonly linked by finer elements, either partial colliculi or dis- sepiments, 0.01—0.02 mm thick. Astrorhizae scattered, discontinuous, irregularly branching segments, ca. 0.6 mm diameter; tabulate, or locally empty; generally, not exclusively, at mamelon summits. Material.—Two fragmentary specimens, one well preserved, one poorly preserved. No growth surfaces preserved. Hypotype GSC 108855. Second specimen 110-132. Discussion. — This species demonstrates similarities to Aculatostroma kaljanum (Bogoyavlenskaya) from the karpinskii horizon (Emsian, gronbergi—inversus Zones; Khodalevich et al., 1982), eastern slope of the northern Urals. Bogoyavlenskaya's (1977) description 15 sketchy, and precludes thorough comparison. Lam- inar spacing of A. kaljanum is noted as 4 per mm, laminar width 0.07—0. 1 mm, and pillar thickness “does not exceed 0.1 mm" (Bogoyavlenskaya, 1977, p.15) The cited thicknesses exceed those of the Ellesmere specimens, but Bogoyavlenskaya's illustration (1977, Plate 4, fig. 1) suggests laminae and pillars approx! mately 0.05 mm thick. Significantly, Bogoyavlenskay4 (1977, p.15) describes the astrorhizae as numerous and simple", and “astrorhizal tabulae numerous, af” p.109), in the generic definition of Plectostroma, “the difference consists (sic) in the connective processes, which in Plectostroma are distributed irregularly, but in Actinostroma they occur on definite levels and form regular, concentric laminae.” Various species, how- ever, demonstrate differing degrees of collicular irreg- ularity versus alignment. At one extreme, the type spe- cies of Plectostroma, P. intertextum (Nicholson, 1886), shows random distribution of colliculi. Other species, such as P. necopinatum Nestor, 1964, show rare col- licular alignment. Near the opposite extreme, species such as P. salairicum have many more colliculi in alignment than are not, a fact that has prompted Khro- mych (1984) to retain P. salairicum in the genus Ac- tinostroma (but see below). Still, a strictly statistical distinction between Plectostroma and Actinostroma (on the basis of proportions of aligned versus unaligned colliculi) would obscure important relationships be- tween species that are clearly related and intergrada- tional in nature. As Stock (1979) has noted, Plecto- stroma represents a useful grouping of species inter- mediate in skeletal element size and spacing between Actinostroma and Densastroma (this latter with a very fine skeletal network). This broader approach follows that of Fligel and Flúgel-Kahler (1968) and Fligel (1974), who initially reassigned Actinostroma salairi- cum Yavorsky to Plectostroma. The assignment by Khromych (1984) of specimens to Actinostroma salairicum Yavorsky is questionable. Khromych’s Siberian specimens have more distantly spaced and thicker structural elements than either Ya- vorsky’s (1930) or those herein (3 to 4 pillars per mm; 5 “laminae” per mm; pillars 0.12-0.15 mm thick; “laminae” 0.08—0.10 mm thick; Khromych, 1984). Fliigel (1974, p. 178) tabulated the major morpho- logic features of six Devonian species of Plectostroma, including P. salairicum. An additional five Devonian species from the former Soviet Union are listed by Bogoyavlenskaya and Khromych (1985). Occurrence. —Bathurst Island, Dyke Ackland Bay; unnamed limestone, lower 100 m; uppermost Emsian/ basal Eifelian (undifferentiated patulus Zone). Genus ACULATOSTROMA Khalfina, 1968 Type species. — Syringostroma verrucosum Khalfina, 1961. Aculatostroma cf. A. kaljanum (Bogoyavlenskaya, 1977) Plate 2, figures 1-5 cf. Coenellostroma kaljanum Bogoyavlenskaya, 1977, p. 15, PI. 4, figs. la, 1b. Description. —Skeleton laminar to gently wavy, up to 10 cm. DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN La tecture. Rather, they appear to be preferentially nucle- ating at latilaminar bases. Where the bands are thickest (especially within the basal layer), their crystalline hab- it is bundled, and their optical characteristics suggest fascicular-optic calcite (sensu Kendall, 1977). This lat- ter is generally considered strictly a void-filling fabric, but in this instance it appears to be displacive (replace- ment). A second specimen, not as well preserved as the one described and illustrated is also assigned to this species. In the second specimen, laminar spacing is slightly closer than in GSC 108855, 7 to 9 per 2 mm, and it displays slightly fewer astrorhizal canals, although equally poorly formed. Occurrence.— Blue Fiord Formation, lower 100 m; Vendom Fiord (GSC 108855), Eids Fiord (one speci- men); lower Emsian (dehiscens Zone). Order CLATHRODICTYIDA Bogoyavlenskaya, 1969 Family CLATHRODICTYIDAE Kühn, 1927 Genus CLATHRODICTYON Nicholson and Murie, 1878 Type species. — Clathrodictyon vesiculosum Nichol- son and Murie, 1878. Clathrodictyon ellesmerense Stearn, 1983 Plate 3, figures 1-3 Clathrodictyon ellesmerense Stearn, 1983, p. 545, 547, fig. 3A-3E, 1989a, fig. 1A. Material. —Twenty-one specimens; poorly to mod- erately well preserved. Hypotypes GSC 108856 to 108858. Other specimens at Geological Survey listed in Appendix 3. Discussion. — This species was established by Stearn (1983) for specimens collected from the lower Blue Fiord Formation in the vicinity of the type section. The majority of specimens of Clathrodictyon elles- merense in this study come from equivalent localities on Ellesmere Island, ranging from dehiscens to gron- bergi Zones (lower Emsian). Additional specimens of C. ellesmerense from the Bird Fiord Formation of Ellesmere Island and from Bathurst Island extend the stratigraphic range of this species to lowest Eifelian. The additional specimens of this study expand the morphological parameters of Clathrodictyon ellesmer- ense from the original description of Stearn (1983). The new specimens demonstrate a greater range of laminar spacing than do those in the original collection (about 11.5 per 2 mm; Stearn, 1983); pillar spacing and the thickness of the skeletal elements are within ranged parallel to laminae", the same condition as in the Ellesmere specimens. Additionally, Bogoyavlen- Skaya noted the occurrence of an “epitheca" (0.5 mm thick) on the undersurface of some specimens; a po- tentially similar structure, a digitate, root-like basal Phase of disordered skeletal material, is present in one Of the Ellesmere specimens (GSC 108855). This last feature, while interesting, is of negligible taxonomic value because it is an abnormal growth phenomenon. Considerable uncertainty has surrounded the generic assignment of species to either of Aculatostroma or Atelodictyon, and whether Aculatostroma itself is an actinostromatid (colliculate laminae) or a clathrodic- tyid (continuous laminae) (see Stearn, 1991). For the Most part the fine structure of Ellesmere ۵ cf A. kaljanum is diagenetically obscured, but a few thin zones of one or two laminae (occurring beneath Sediment interlayers) preserve skeletal elements in ex- treme detail. Plate 2, figures 4 and 5 depict the colli- Culate pillars found in such a zone; note how the col- liculi arise sharply, parasol-like, off the short pillars. The astrorhizae of Aculatostroma cf. A. kalianum are unusual in their disordered arrangement, abun- dance of near-horizontal tabulae or cysts, and apparent facultative association with mamelons. It is possible that they instead represent intergrowths of commensal Or parasitic organisms. Plate 2, figure 3 presents sup- Plementary evidence to suggest that the tubes are in- deed astrorhizal canals, albeit aberrant ones; on this Slabbed, tangential surface, the tubes can be seen to Tadiate from a central area, branching dichotomously and slightly thinning outward. Such a horizontal pat- tern is inconsistent with the commensal habit of a foreign organism (such as Syringopora), and the abun- dant horizontal tabulae mitigate the possibility of an Invading borer. The common occurrence of these tubes In the arctic specimens and those from the Urals IA. aljanum (Bogoyavlenskaya)] implies that the struc- Ures are intrinsic to the stromatoporoid, rather than A the product of a chance guest or invading organism. The preservation of the Ellesmere specimens de- Serves some additional mention. As noted in the de- Scription, skeletal elements (laminae, pillars, dissepi- Ments, tabulae) are commonly thickened, in some Specimens by as much as 10 times the original thick- Ness, Periodic, thick (0.5-1.0 mm), dark bands parallel © laminae in specimen GSC 108855, and they are confluent with, and appear to be composed of, the same Material as the skeletal elements. The dark bands, of genetic origin, occur at the same periodicity as la- “laminar boundaries (elsewhere indicated by thin sed- Ment interlayers). In thin section, ghosts of skeletal p ments are discernable within the thick bands, i.e., * bands are not part of the original skeletal archi- BULLETIN 349 Surfaces poorly exposed, apparently bearing numer- ous, small mamelons. Latilaminae common, thickness 0.7-1.0 cm. Vertical section: Laminae continuous, flat or gently undulate, less commonly highly undulate-to-irregular; thin, 0.03 to 0.04 mm, rarely to 0.05 mm; in specimens with syringoporids, deflected slightly downward at cor- allite margins. Laminar spacing very close, but highly variable; species range 9 to 18 per 2 mm, commonly 13 to 16 per 2 mm; holotype GSC 108859 average 15.2 (n=20) range 13 to 18, paratype GSC 108860 average 15.5 (n=10) range 13 to 17, paratype GSC 108862 average 14.2 (n=10) range 13 to 16. Successive phases of laminar spacing common, 1.5 to 2.0 mm thick, or about four to five phase-cycles per latilamina; where closely spaced, rare pairs of laminae may be tightly adpressed, separated by gap of 0.01 to 0.02 mm. Basal phase of stringy material 0.2 to 0.3 mm thick at base of latilaminae, also as thin lenses irregularly through- out skeleton; some latilaminar surfaces show minor erosion (truncated or missing upper laminae). Pillars thin, 0.02-0.04 mm; generally superposed through in- terval of 2 to 10 laminae, although readily lost to dia- genesis; dominantly simple, straight, rod-shaped; a few slightly thickened or apparently split upward; spacing variable, generally very close and regular, species range 11 to 20 per 2 mm, commonly 13 to 17 per 2 mm, holotype average 16.5 (n=20) range 14 to 20, paratypes GSC 108860 average 15.0 range 13 to 17, GSC 108861 average 13.5 range 12 to 15, GSC 108862 average 15.1 range 13 to 17 (all n=10); tending to be closer where laminae closely spaced. Astrorhizae variably present, common or abundant in most specimens, in a few rare or absent, consisting of central bundle of few vertical canals 0.1 to 0.2 mm diameter, and many smoothly curved lateral branches merging into galleries; asso- ciated with shallow mamelons, vertically persistent uP to full latilaminar height; pervasive lateral branches 5 small circular gaps 0.2 mm diameter or short tubes locally interrupting laminae, abundant near axis and along certain levels; absent or imperceptible in speci- mens with commensal syringoporids. Dissepiments uncommon except in areas of skeletal repair. Skeletal microstructure compact, minutely speckled; some specimens irregularly fibrous. Tangential section: Laminae dense meandriform bands. Pillars commonly small dots, 0.02-0.04 mm diameter, or short vermiform strands; closely spaced, about 0.04 mm apart. Astrorhizae axial bundle of three to five canals and surrounding dense array of outward- branching lateral canals; canal width 0.1 to 0.2 mm; complexity and density highly variable between spec imens, closest center-to-center spacing about 5 mm. Material.—Twenty-four specimens, mostly well- the originally cited ranges. In the additional specimens, laminar spacing ranges from about 10 to 15 per 2 mm, with the majority of specimens measuring 10 to 12 laminae per 2 mm. Specimens with especially closely spaced laminae may demonstrate these distinctive features: 1) repeated variations in laminar spacing (=successive phases); and 2) local development of vertically impersistent papil- lae. Of the 13 specimens of Clathrodictyon ellesmer- ense from the lower Blue Fiord Formation, two display successive phases of growth in which laminar spacing changes from a minimum of 8 per 2 mm progressively up to 16 per 2 mm, over vertical distances of 3 to 5 mm (PI. 3, fig. 1). Such rhythmic changes may indicate seasonal variation in growth rate (Stearn, 1989a). An- other two of the Blue Fiord specimens of C. ellesmer- ense display discrete protuberances measuring 1-2 mm wide by 2-3 mm high (PI. 3, fig. 3). They are formed as small domal inflections of the laminae and are ver- tically limited and not associated with astrorhizal ca- nals. In thin section, no distributional pattern of the protuberances is readily apparent within the skeleton, but one hand-specimen suggests they occur at growth interruptions, and may be an intrinsic response to un- favourable environmental conditions. As noted earlier by Stearn (1983), some specimens of Clathrodictyon ellesmerense display dense inter- growths of syringoporid corals. Occurrence. — Blue Fiord Formation; lower 100 m, type area (15 specimens); lower member, Vendom Fiord (two specimens); lower Emsian (dehiscens-gronbergi Zones). Blue Fiord Formation, upper member, Ven- dom Fiord (one specimen); Disappointment Bay For- mation, Truro Island (one specimen); inversus Zone. Bird Fiord Formation, Ellesmere Island, type area (one specimen); Northeastern Bathurst Island, unnamed limestone formation (one specimen); highest Emsian- basal Eifelian (undifferentiated patulus Zone). Genus GERRONOSTROMA Yavorsky, 1931 Type species. — Gerronostroma elegans Yavorsky, 1931. Gerronostroma septentrionalis, new species Plate 3, figures 4, 5: Plate 4, figures 1-4 Gerronostroma sp. A Stearn, 1983, p. 547-548, figs. 4A, 4B. Diagnosis. —Thin laminae, closely but variably spaced 9 to 18 in 2 mm; pillars thin, spaced regularly and closely, 11 to 20 in 2 mm; dissepiments uncom- mon. Description. —Skeletal form variable, laminar to weakly domical, commonly irregular, rarely bulbous. DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 19 from the Stuart Bay Formation, Bathurst Island, none is closely comparable to G. septentrionalis n. sp. About one-third of the specimens of Gerronostroma septentrionalis n. sp. exhibit dense intergrowths of a syringoporid coral (e.g. Pl. 4, fig. 3). The intergrown corallites are either very abundant or completely ab- sent, i.e., there is no intermediate condition of just a few intergrown corallites. This implies that the rela- tionship between the coral and G. septentrionalis n. sp. is neither accidental nor parasitic, for which a grada- tion of intergrowth densities should occur. Mutualism is unlikely, as Gerronostroma specimens without the coral are abundant and show no obvious signs of lesser growth than those with the coral. Rather, strict com- mensalism on the part of the coral is indicated. Gerronostroma septentrionalis n. sp. is commonly found competitively overgrowing other stromatopo- roid species (primarily Stromatopora polaris Stearn and Stictostroma? nunavutense n. sp.). A third of the spec- imens demonstrate this overgrowth, and of these, three specimens (including the holotype) show intimate in- terfingering of the competing stromatoporoids. In the holotype (GSC 108859), at least five such interfingering episodes occur within one latilamina of G. septentrion- alis n. sp. (Pl. 4, fig. 4). The overtopping/recolonization by Gerronostroma is in each instance clearly defined by a characteristic mat of basal stringy tissue. By the end of the latilaminar event, the competing species appears to have been excluded from the holotype spec- imen, and indeed in each example observed Gerron- ostroma ultimately overgrows the other in vertical suc- cession. Etymology. —Latin septentrionalis, of, or from the north. Occurrence. — Blue Fiord Formation, lower mem- ber; Ellesmere Island, vicinity formation type area (21 specimens), Vendom Fiord (two specimens); lower Emsian (dehiscens Zone). Uppermost Eids Formation, Eids Fiord, Ellesmere Island (one specimen); lower Emsian (dehiscens Zone). Genus PETRIDIOSTROMA Stearn, 1992, (nom. subst. pro Petrostroma Stearn, 1991 non Petrostroma Dôderlein, 1892) Type species. — Simplexodictyon simplex Nestor, 1966. Petridiostroma sp. Plate 5, figures 1-2 2 Anostylostroma laxum Nicholson. Stearn, 1990, p. 503-504, figs. 3.3—3.5. Description. —Skeleton laminar to irregular. Lati- laminae about 5 mm thick evident in some specimens. preserved. Seven specimens with commensal syrin- 80porids, seventeen without. Holotype GSC 108859; Paratypes GSC 108860 to 108862. Other specimens listed in Appendix 3. Discussion. — Gerronostroma septentrionalis n. sp. demonstrates extremely broad variation in laminar and Pillar spacing, astrorhizal arrangement and abundance, and overall growth form. It is the same species rec- ognized earlier by Stearn (1983) as Gerronostroma sp. A (also from the lower Blue Fiord Formation, Elles- Mere Island). Minor differences between the earlier description and this one are attributable to the broad Specific variation of G. septentrionalis n. sp., not fully Tepresented in the small collection of Stearn (1983). The earlier description noted the astrorhizae as being Inconspicuous and latilamination as not prominent, Which by the present species-concept are more excep- tions than the norm. The pillar spacing cited by Stearn (1983), 11 to 12 per 2 mm, is within the range of G. Septentrionalis n. sp., although low; laminar spacing for G. sp. A Stearn, 1983, is 16 to 18 per 2 mm. The New specimens of G. septentrionalis n. sp. demonstrate Toughly a one-to-one ratio of pillar to laminar spacing (for any specimen or uniform region within a speci- Men). The apparent disparity exhibited by the speci- Mens of Stearn (1983) is due to preferential diagenetic loss of pillars, a feature consistently evident in both Collections. Some specimens show partial or complete Temoval of pillars, leaving only the closely spaced lam- Mae intact. Another specimen referred by Stearn (1983) to Ger- l'onostroma cf. G. immemoratum Bogoyavlenskaya is Not conspecific with Gerronostroma septentrionalis n. SP. Its laminar and pillar spacings are well outside the Tange of G. septentrionalis n. sp. and, moreover, its Skeletal element thicknesses are much greater. Consid- ering the geographic and stratigraphic similarity of the Collection of Stearn (1983) and those herein, the ab- Sence of new specimens similar to G. cf. G. imme- Moratum is puzzling. Still, the species appears to be Valid, and the paleogeographic relationship to the east- ern Urals suggested by G. cf. G. immemoratum is sup- Ported by the present evidence (see under occurrence of Aculatostroma cf. A. kaljanum, p. 17). G. septentrionalis n. sp. shows little similarity to ot er known species of Gerronostroma. Two lower Em- Slan species are described by Lessovaya (1970) from © Zeravshan Range, Uzbekistan: Gerronostroma is- ini schirdagica Lessovaya has much thicker skel- al elements, more widely spaced, than G. septentrion- a ب‎ n. Sp.; and Gerronostroma uralicumforme Lesso- Ya appears more reasonably to belong to Atopostro- = Yang and Dong. Of the three upper Lochkovian Pecies of Gerronostroma described by Stearn (1990) BULLETIN 349 1985) is best assigned to the genus Schistodictyon (pil- lars branch upward dichotomously) (Stearn, 1991). Occurrence. —Blue Fiord Formation, Ellesmere Is- land; Goose Fiord, dolomitic facies (one specimen), mid-Emsian (inversus Zone); Vendom Fiord, near base of upper member (two specimens), lower Emsian (in- versus Zone). Genus ATELODICTYON Lecompte, 1951 Type species. —Atelodictyon fallax Lecompte, 1951. Atelodictyon cf. A. solidum Khromych, 1976 Plate 5, figures 3,4 cf. Atelodictyon cylindricum solidum Khromych, 1976, p. 48, pl. IV, figs. 4a, 4b, 4c. Description. —Fragmentary; skeleton laminar. Vertical section: Laminae thin, 0.02—0.03 mm, lo- cally thickened to 0.05 mm; mostly continuous, but locally broken, due either to poor preservation or pen- etration by astrorhizal canals; spaced 4 to 5 per 2 mm; irregularly undulate, interlaminar spaces locally swol- len or pinched out. Coenosteles complex, thin; dom- inantly vertical, but irregularly sinuous, crumpled. Two types of coenosteles occur (with numerous intergra- dational forms): dominantly 1) thin, 0.02-0.04 mm, tightly crowded, paired or in interwoven hairlike bunches, commonly splaying upward to meet overly- ing lamina; subordinately 2) thicker, up to 0.10 mm, thickening or splitting upward to meet lamina. Coe- nostele spacing 8 to 11 per 2 mm, average 9.5 (n— 10), but locally tightly crowded and individuallly indis- cernable. Astrorhizae large, extensive, composed axi- ally of vertical bundles of canals, each 0.4-0.5 mm wide, spread laterally like buttressed roots of a tree, astrorhizal tributaries widely scattered, form hollow circles or short tubes, commonly truncating laminae. Dissepiments uncommon, thin, broadly convex, most- ly preservationally obscured. Microstructure probably compact. Tangential section: Coenosteles vermiform to net- like; thickness variable, 0.03-0.08 mm; rarely dots 0.02-0.05 mm diameter; rarely irregularly ring-shaped; where netlike, enclosing galleries 0.2-0.5 mm across: Astrorhizae large, very prominent, axial canal diam- eter 0.4-0.5 mm; at optimal height of section forming rosettes, comprising a central bundle of 5 to 6 vertical canals, surrounding array of long ramifying lateral ca- nals extending up to 1.5 cm; tributary canal segments 0.2-0.3 mm diameter scattered throughout skeleton central canal margins generally well-defined, tributary canals less defined, merge into skeletal network. Dis“ tance between astrorhizal centres about 1.0 cm. Material.—Two specimens, one moderately well Vertical section: Laminae continuous, gently un- dulate; 0.04—0.06 mm thick, commonly 0.05 mm thick; spaced 6 to 8 per 2 mm, specimen averages 7.5 (GSC 108863), 6.3 (GSC 108864) (each n=10); microstruc- ture compact. Pillars simple, commonly rod-shaped, some slightly thickening upward to meet overlying lamina, rarely branching upward; 0.04—0.08 mm thick, average 0.055mm (GSC 108863; n=20); variably spaced, 7 to 11 per 2 mm, specimen averages 8.8 (GSC 108863), 8.5 (GSC 108864) each n=10; arrangement between successive laminae irregular, random, pillars neither consistently staggered nor superposed; locally absent for lengths up to 1.0 mm. Dissepiments com- mon, broadly convex; thin 0.02 mm. Tangential section: Pillars solid dots 0.04—0.08 mm diameter; rarely incomplete small circles with clear center, diameter up to 0.12 mm. Dissepiments con- spicuous, shallow arcs or irregular segments bridging pillars. Astrorhizae absent. Material. —Three specimens, ranging from poorly to moderately well preserved. Hypotypes GSC 108863, 108864. Other specimen 111-1. Discussion. — These few specimens from Ellesmere Island are best assigned to the genus Petridiostroma (Stearn, 1992) on the basis of their planar laminae and predominantly simple pillars. They are quite similar to specimens from the upper Lochkovian of Bathurst Island (“Stuart Bay” Formation) referred to Anosty- lostroma laxum by Stearn (1990). The Bathurst Island specimens have more distantly spaced laminae (ten- count average of 5.5 in 2 mm in one specimen, 7.1 in the other) and pillars (ten-count average of 5.5 in 2 mm in one specimen, 6.2 in 2 mm in the other) than do those described here, but they are otherwise closely comparable. In light of recent study (Stearn, 1991), Anostylostroma should be restricted to species in which the majority of pillars branch-upward irregularly and complexly. As such, the Lochkovian specimens re- ferred to Anostylostroma laxum by Stearn (1990) should be reassigned to Petridiostroma. These Lochkovian specimens show a predominance of simple pillars, and only a few are Y-shaped (Stearn, 1990). Re-examina- tion of the specimens reveals that less than one per cent of the pillars branch, a proportion comparable to the Ellesmere Island Petridiostroma sp. specimens. Tangential sections are especially diagnostic, for al- though the few branched pillars appear prominent in vertical section, tangentially the overwhelming major- ity of pillars are dots. Nonetheless, more specimens of the Ellesmere Island Petridiostroma sp. are needed to support a definite relationship to the Lochkovian spec- imens. Anostylostroma laxum (Nicholson, 1887) itself (cf. e.g., Fagerstrom, 1982; Bjerstedt and Feldmann, DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 21 of this species are attributable to preservation (see be- low) and, moreover, to interruption by the pervasive astrorhizal system. Most importantly, the coenosteles (pillars) in vertical detail show no evidence of becom- ing colliculate at their tops; they mostly either splay apart into fine strands, or thicken to meet the lamina above, against which they are sharply abutted. Atelodictyon cf. A. solidum exhibits unusual pres- ervation, although common for other stromatoporoids from the same locality (the shallow-platform, dolo- mitic facies of the Blue Fiord of southwesternmost Ellesmere Island). Intraskeletal galleries of A. cf. A. solidum are filled with early-stage, opaque calcite ce- ment, which is poorly transparent in thin-section. When viewed in transmitted light, skeletal elements and ce- ment-filled galleries are nearly equally opaque, and in- distinguishable. Examination and illustration of this species therefore had to be done in reflected light, which accounts for the murkier appearance of Pl. 5, figs. 3 and 4 compared to others. Occurrence. — Blue Fiord Formation, Muskox Fiord, Ellesmere Island; mid-Emsian (inversus Zone). Family TIENODICTYIDAE Bogoyavlenskaya, 1965 Genus ANOSTYLOSTROMA Parks, 1936 Type species. — Anostylostroma hamiltonense Parks, 1936. Anostylostroma anfractum, new species Plate 6, figures 1-5 Diagnosis. —Laminae thin, spaced 7 to 10 in 2 mm; pillars variable, complexly upwardly branched or joined, distinctive in form in tangential section as short chains, geniculate strands, and triskelions. Description. —Skeleton laminar to slightly domed. Vertical section: Laminae continuous, gently un- dulate; thin, 0.03—0.04 mm, locally thickened to 0.05— 0.06 mm; regularly spaced, 7 to 10 per 2 mm, specimen averages 9.2, 8.6, 9.5, 7.2 (GSC 108866 to 108869; each n=10); microstructure transversely fibrous or lo- cally transversely porous. Pillars highly variable, most- ly upward-branching, either irregularly or simply (Y- shaped); a few upward-thickening or rod-shaped; com- monly confined to single interlaminar interval, a few superposed over 2 to 4 laminae. Pillar thickness 0.03— 0.08 mm, commonly 0.05-0.06 mm; may thicken up- ward to as much as 0.20 mm at overlying lamina; spaced 7 to 10 per 2 mm, specimen averages 7.6, 8.8, 8.5, 9.0 (GSC 108866 to 108869; each n=10). Dissep- iments common, generally not abundant; thin, 0.02 mm, long, broad, sub-horizontal, gently convex. La- tilaminae absent, but thin (0.5-1.0 mm) basal phases Preserved (GSC 108865), one poorly preserved (120- 6). Discussion.—These few but distinctive specimens Compare favorably with Atelodictyon solidum Khro- mych, 1976, known from the Emsian of the Ulakhan- Sis Range, northeastern Siberia. Khromych (1976) not- ed the following characteristics of A. solidum: laminae 0.05 mm thick, spacing 5 to 10 per 2 mm; pillars 0.04- 0.07 mm thick, spacing 10 per 2 mm: astrorhizal canals 0.55 mm wide, distance between neighboring astro- thizae 9.1 mm. Morphometric differences between this and the Ellesmere specimens are therefore minor, with the possible exception being the more closely spaced laminae of Siberian A. solidum. Shared features of pri- Mary importance are the nature and disposition of the Coenosteles, and particularly the large, pervasive as- trorhizae, which are identical in the Siberian and Elles- Mere Island specimens. Any reservation expressed in the assignment of the Ellesmere specimens is princi- Pally due to the limited material available, rather than to Morphologic differences, which are within an ac- ceptable range of specific variability. Atelodictyon solidum was originally described as a Subspecies 4. cylindricum solidum Khromych, 1976. Atelodictyon cylindricum Khromych, 1971 is an un- Usual species with a cylindrical or spherical growth form; it occurs in the Lower Devonian (?Lochkovian- Tagian) Nelyudimskaya Suite of the Omulevski Ountains, northeastern Siberia. In consideration of age and morphologic differences, we elevate A. c. so- ‘dum Khromych, 1976 to species level. The exact age of Atelodictyon solidum Khromych is Uncertain, Khromych (1976, p. 48) lists it as “Eifelian Stage, lower Tababastaakhskaya Subsuite, Ulakhan-Sis ange.” Traditionally Soviet geologists have set the „ OWer-Middle Devonian boundary much lower than In the West, in what is now considered Emsian. Only relatively recently have Soviet/Russian stratigraphers adopted international boundary-placements (cf. zhonsnitskaya, 1988). An additional complication With the northeast-Siberian material is that Khro- Mych's (1974, p. 71-73; 1976, p. 40) correlations are mm almost entirely on stromatoporoids alone, un- i Pported by other fossil groups. Allowing for these sui tainties, the age of the Tababastaakhskaya sub- "e appears to be Emsian, probably mid-to-late Em- e N, therefore comparable to the inversus Zone prov- ance of the Ellesmere specimens. "age to the apparent incompleteness of the laminae ^ telodictyon cf. A. solidum, consideration was given ha an assignment to the actinostromatid genus Acu- Stroma (which also has vermiculate to cateniform E in tangential section; cf. Stearn, 1991). As noted € description above, discontinuities in the laminae | | | | BULLETIN 349 Pseudoactinodictyon conglutinatum, new species Plate 7, figures 1-4 Diagnosis. —Laminae thick, compounded of fusion of adjacent thin laminae, locally split like those of Sim- plexodictyon, widely spaced 2 to 4 in 2 mm; pillars robust, spooled or dividing upward, dotlike of sausage- shaped in cross section. Description. —Skeleton domal to hemispherical, up to 10 cm diameter. Surface irregular, without percep- tible mamelons or astrorhizae. Vertical section: Laminae undulate; spacing wide, inconsistent, 2 to 4 per 2 mm, holotype (GSC 108870) average 3.3 (n=10); distance between successive lam- inae variable, commonly 0.30-1.40 mm, holotype (GSC 108870) average 0.65 mm range 0.40-1.00 mm (n=30), paratype (GSC 108871) average 0.76 mm range 0.35— 1.35 mm (n=30), locally as much as 2.0 mm. 6 compound, formed by fusion of adjacent thin laminae, either completely or incompletely; completely fused laminae thick 0.14-0.28 mm average 0.20 mm (n—20, combined GSC 108870 and 108871), no axial zone; incompletely fused twin laminae separated by thin gap ca. 0.02 mm, locally swollen forming flat-bottomed vacuities, lower twin lamina generally thinner 0.04- 0.06 mm than upper twin 0.12-0.16 mm; laminae lo- cally perforate, perforations/foramina occluded by dis- sepiments at or near laminar level. Pillars commonly simple spool-shaped, or upward-dividing Y-shaped; thick 0.12-0.20 mm, holotype (GSC 108870) average 0.13 mm paratype (GSC 108871) average 0.17 mm (each n=10); spacing variable, range 4 to 8, commonly 5 to 7 per 2 mm, holotype (GSC 108870) average 5.5 per 2 mm (n=20), paratype (GSC 108871) average 6.6 per 2 mm (n=10). Dissepiments common, locally abundant. Microstructure compact. Astrorhizae ob- scure, indicated only by vaguely defined zones of downturned laminae, inwardly inclined pillars, dens¢ concentrations of dissepiments and laminar perfora- tions. Tangential section: Pillars solid dots 0.10—0.14 mm diameter, or thicker, irregular, sausage-shaped or con- fluent (toward upper laminae). Dissepiments common, locally abundant, linking just less than half of pillars. Interlaminar gaps and vacuities scattered but promi- nent, more prevalent/conspicuous than in vertical sec" tion. Material. — Three partial skeletons, moderately well preserved. Holotype GSC 108870, paratype GS 108871, specimen 111-19. Discussion. — Compared to Middle Devonian spe- cies of Pseudoactinodictyon, P. conglutinatum n. SP: displays generally thicker structural elements and wid- er laminar spacing. The most closely comparable spe“ cies are P. juxi Flügel, 1958 from the Givetian of Sauer" of unordered skeletal material may occur overlying growth interruptions. Tangential section: Laminae moderately dark bands, mostly 0.1-0.2 mm wide; gently meandering. Pillars isolated or interconnected strands, uniformly thick 0.02 mm diameter; strands commonly geniculate, com- posed of short straight portions (about 0.2 mm long) turning sharply at obtuse angles; shapes commonly ap- proach a triskelion; a few strands interconnected, but not for great lengths; some isolated oblique or circular dots, 0.02 mm diameter, may be locally abundant; very rarely form irregular rings. Pillar microstructure trans- versely fibrous. Astrorhizae absent. Material. — Four fragmentary specimens. Preserva- tion mediocre to moderately well preserved. Holotype GSC 108866. Paratypes GSC 108867 to 108869. Discussion. — Anostylostroma anfractum n. sp. is most clearly distinguished in tangential section by its pillars, which appear as angular, geniculate strands forming: triskelions, short chains, or isolated masses. It has the most complex pillar arrangement of any species of An- ostylostroma, which typically exhibit short vermiform pillars in tangential section. The pillars of Anostylos- troma confluens Galloway and St. Jean, 1957, from the Givetian of Indiana, approach this form, but are not as interconnected as those of A. anfractum n. sp. The cross sections of the pillars of A. confluens cut in tangential section are short, vermiform or coalescing, and without the geniculate form of A. anfractum n. sp. The regularity of pillars in tangential section belies the extreme variability of pillars in vertical sections of A. anfractum n. sp. Two factors complicate character- ization of pillars in vertical aspect: generally mediocre preservation, and variation in proportions of different pillar types between specimens. In vertical section, two of the paratypes (GSC 108868 and 108869) exhibit the commonest pillar arrangement, dominated by com- plexly branching, irregular, commonly inclined pillars. A third paratype (GSC 108867) in contrast displays a more orderly arrangement of pillars, in which simple rods are comparatively common (Pl. 6, fig. 3). The holotype (GSC 108866) represents an intermediate case, with complex and simple pillars occurring in near equal proportions. Etymology. — Latin anfractum: bending, winding, or circuitous. Describes the pillars in tangential section. Occurrence. — Northeastern Bathurst Island; un- named limestone formation, lower 100 m; highest Em- sian/basal Eifelian (undifferentiated patulus Zone). Genus PSEUDOACTINODICTYON Flügel, 1958 Type species. — Pseudoactinodictyon juxi Flügel, 1958. DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 23 “bipartite” laminae with an axial light-coloured zone (Lessovaya, 1970; p. 87). Lessovaya’s description and illustrations do not however indicate any divergence or gaps between the compound or “bipartite” laminae; the pillars of S. grandiosum are thick, simple and spool- shaped. It appears unlikely that Pseudoactinodictyon conglutinatum n. sp. and Simplexodictyon grandiosum are the same species, but that the central Asian species may be another Lower Devonian form of Pseudoac- tinodictyon, allied to Pseudoactinodictyon conglutina- tum n. sp. An earlier suggestion by Stearn (1991) that Simplexodictyon grandiosum should be reassigned to the genus Petridiostroma is probably incorrect. Etymology.—From the Latin conglutinatus, bound or glued together; describes the fused twin laminae. Occurrence. — Blue Fiord Formation, Ellesmere Is- land; formation type section, upper member, from a unit lying 200-400 m below the top of the formation (two type specimens); upper Emsian (inversus-serotin- us Zones). Bird Fiord Formation, near base of for- mation; Bird Fiord, Ellesmere Island (one specimen); uppermost Emsian/basal Eifelian (undifferentiated pa- tulus Zone). Genus SCHISTODICTYON Lessovaya, 1970 Type species. — Schistodictyon posterius Lessovaya, 1970. Schistodictyon? sp. Plate 7, figures 5,6 Description. —Skeleton apparently laminar. Vertical section: Laminae thin 0.03—0.04 mm, reg- ular, continuous, flat or gently undulate; spacing reg- ular, 7 to 10 per 2 mm, average 8.6 (n=10); micro- structure compact, locally weakly transversely fibrous. Pillars very variable: simple spool-shaped (44%), up- ward-thickening to meet overlying lamina (28%), up- ward-bifurcating Y-or V-shape (26%); doubly upward- dividing (2%) (n=100); dominantly vertical, but com- monly inclined; spaced 7 to 9 per 2 mm, average 7.7 (n=10); thickness 0.04—0.06 mm, up to 0.10 mm at junction with overlying lamina; rarely superposed. Tangential section: Laminae form thin, diffuse, me- andering bands. Pillars dominantly simple dots 0.04— 0.08 mm diameter, may be vermiform or linked to- ward laminae; irregular rings rare. Dissepiments rare. Astrorhizae absent. Material. — A single specimen, GSC 108872. Well preserved. Discussion.—This single specimen is questionably assigned to the genus Schistodictyon on the basis of its Y-and V-shaped pillars (a few of which are doubly bifurcating). Ideally, Schistodictyon is characterised by land, Germany (Fligel, 1958), and P. vagans Parks, 1936 from the Detroit River Group (probably Emsian) of Ontario and Ohio (Fagerstrom, 1982). The spacing of both laminae and pillars is roughly one and one- half times denser in P. vagans than in P. conglutinatum D. sp., and skeletal elements are finer (P. vagans lam- mae 0.05-0.07 mm, pillars 0.05-0.10 mm thick). Pillar thickness of P. juxi is comparable to P. conglutinatum D. Sp., and ranges of laminar thicknesses overlap (0.10- 0.20 mm vs. 0.14-0.28 mm); spacing of skeletal ele- ments is somewhat closer in P. juxi (4 to 6 laminae, 6 to 8 pillars in 2 mm). The most noteworthy feature of Pseudoactinodictyon Conglutinatum n. sp. is the arrangement of successive laminae, either fused to form thick compound laminae, Or separated by a gap of irregular thickness. Such an arrangement suggests a growth pattern in which each Successive unit, composed of thin upper and lower laminae joined by pillars, is separated by an interrup- tion in growth. The succeeding thin lower lamina is lain atop the upper lamina of the previous growth unit, and either “welded” to it, or remains separated by a Sap. This unusual growth pattern is also known in (and Characteristic of) the genera Simplexodictyon (formerly Diplostroma; cf. Nestor, 1976; Stearn, 1991) and Nur- Atodictyon (known from only one specimen; Lesso- vaya, 1972, Stearn, 1980). The significance of such gaps between the laminae is further discussed by Stearn and Pickett (1994). Mori (1968) first recognized that the “split” laminae of Simplexodictyon indicate pauses growth, the gaps being devoid of skeletal elements and often incorporating trapped sediment or encrust- Mg organisms. No trapped sediment or encrusting or- 8anisms are present within the interlaminar gaps of P Seudoactinodictyon conglutinatum n. sp. Another dif- ference from Simplexodictyon is that in this latter ge- Nus divergent laminae are much more common than fused laminae, but in P. conglutinatum n. sp. gaps are distributed sporadically: in the paratype (GSC 108871) gaps are much rarer than in the holotype (GSC 109970). Stearn (1980, 1991) proposed the Family Simplex- Odictyidae (formerly Diplostromatidae) for species emonstrating the interrupted growth pattern diag- Dostic of Simplexodictyon and Nuratodictyon. Recog- ‘ition of this unusual growth pattern outside these two Senera, as is the case here, may require reevaluation Or some redefinition of the Family Simplexodictyidae. Simplexodictyon grandiosum Lessovaya, 1970 from © upper Emsian (Favosites regularissimus Zone) of i Zbekistan (Lessovaya, 1970), shows certain similar- lies to Pseudoactinodictyon conglutinatum n. sp. from lesmere Island, and may be related. Simplexodictyon šľandiosum is very robustly built (laminae and pillar SPacings 4 to 5 per 2 mm), and has thick (0.2-0.4 mm), | | BULLETIN 349 ameter, 4-5 mm center-to-center distance. Latilami- nae moderately well developed, 2-4 mm thick. Vertical section: laminae continuous, flat or very gently undulate, consistently parallel; regularly spaced, commonly 13 to 15 per 2 mm, specimens GSC 108873 average 14.3 range 12 to 17, GSC 108177 average 14.2 range 12 to 16, GSC 108176 average 14.0 range 13 to 15, GSC 108874 average 13.8 range 12 to 15 (all n=10); thickness 0.03-0.06 mm, commonly 0.04-0.05 mm; microstructure ordinicellular, transverse tubules and intervening skeletal material both about 10-15 um wide, grading locally to tripartite or with median row of cellules; diagenetically altered laminae tripartite, with median pale band 0.02—0.04 mm thick and dark ex- terior bands 0.01 mm thick, vaguely transversely fi- brous. Pillars stout, spool-shaped, 0.04-0.08 mm thick, thickening and merging into laminae; very rarely formed by up-arching and merger of lower lamina (in the manner of Stromatoporella); irregularly offset be- tween successive laminae, rarely superposed; spaced irregularly 7 to 12 per 2 mm, specimens GSC 108873 average 9.2 range 7 to 11 (n=20), GSC 108177 average 9.6 range 8 to 11 (n=10), GSC 108176 average 9.7 range 9 to 11 (n=10), GSC 108874 average 10.1 range 9 to 12 (n=10); locally absent for lengths up to 1 mm, microstructure poorly preserved, generally suggesting cellules or vertically-aligned tubules. Dissepiments broadly convex, very thin, 5-10 um, commonly oc- cupying uppermost portion of galleries; easily lost dia- genetically, probably originally common. Mamelons variably and only sparingly evident (despite promi- nence on exposed surfaces), apparent in some speci- mens and not in others; mostly shallow, vertically im- persistent, with no or very weak astrorhizal canals; less commonly may be vertically persistent up to 5 mm height, with poorly developed astrorhizae, central ca- nal 0.15 mm wide. Intergrown organisms (corals, algae) common. Tangential section: laminae thick diffuse bands. Open gallery space generally comprises less than half total area. Pillars subcircular, isolated, numerous, crowded, 0.04-0.10 mm diameter; ring-pillars absent; micro- structure cellular (sectioned transverse tubules), cellule diameter 10-15 um, but fine-structure only very rarely preserved, commonly compact. Astrorhizae comprise few, short, poorly-defined canals, 0.10 mm diameter, about half of all mamelon centers without ۰ Material. — Eight specimens; one complete skeleton, 7 partial (2 of which are encrusting). Moderately well to well preserved. Hypotypes GSC 108873 to 108875. 108176, 108177. Other specimens listed in Appen- dix 3. Discussion. — Stictostroma gorriense has been widely recognized from southern Ontario; the most thorough synonymy to date was provided by Fagerstrom (1 982, a predominance of bifurcating pillars (Stearn, 1991), as demonstrated by S. papillatum (Parks) (cf. Stearn, 1991, fig. 2.2). In vertical sections of Schistodictyon? sp. from Ellesmere Island, only about one-quarter of the pillars are bifurcating; about one-half are simple rods and the remainder are intermediate in nature (i.e., upward-thickening). Specimens such as this, which show characteristics intermediate between Schistodic- tyon and related genera such as Petridiostroma and Anostylostroma, are not unusual. Because the true mor- phological range of this species cannot be understood from a single specimen, the generic assignment must remain equivocal. Vertical sections of Schistodictyon? sp. are similar to those of Petridiostroma sp. (also from the Blue Fiord Formation, Ellesmere Island). The main difference 1s the proportion of bifurcating pillars (which are rare in Petridiostroma sp.). Tangential sections more clearly show this distinction, but the possibility cannot be dismissed that the single specimens separately assigned to Schistodictyon? sp. and Petridiostroma sp. are con- specific. Many more specimens are needed before these problems can be meaningfully resolved. Specimens from the Emsian of eastern Australia as- signed to Schistodictyon sp. by Webby and Zhen (1993) are quite similar to the Blue Fiord specimen, but again too little material is available from which to draw firm conclusions. Occurrence. — Blue Fiord Formation, lower 100 m; vicinity type section; lower Emsian (dehiscens Zone). Order STROMATOPORELLIDA Stearn, 1980 Family STICTOSTROMATIDAE Khalfina and Yavorsky, 1973 Genus STICTOSTROMA Parks, 1936 Type species. — Stictostroma gorriense Stearn, 1995. Stictostroma gorriense Stearn, 1995a Plate 8, figures 1—5 non Stromatopora mammillata Nicholson, 1873, p. 94, pl. 4, fig. 4. Stictostroma mammillatum (Nicholson). Parks, 1936, p. 78-81, pl. 14, figs. 3-6. Stictostroma mamilliferum Galloway and St. Jean, 1957, p. 125- 127, pl. 6, figs. 4a,b; Galloway, 1957, pl. 31, fig. 6, pl. 33, fig. 9; St. Jean, 1962, p. 188—189, pl. 31, figs. 1-5; Fagerstrom, 1982, p. 40-41, pl. 8, figs. 6,7; Prosh and Stearn, 1993, figs. 3c, 3d. Stictostroma mccannelli Fagerstrom, 1961, p. 7, pl. 2, figs. 7-9; 1982, p. 40-41. Stictostroma gorriense Stearn, 1995a, p. 26, figs. 1.6, 1.7, 2.5, 2.6; 1995b, p. 1-3. Description. —Skeleton weakly domical to thick- laminar with ragged edge; rarely encrusting or inter- grown. Surfaces bearing abundant, small, very regu- larly spaced mamelons, ca. 1 mm high, 1-2 mm di- DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 29 Table 1.—Comparative measurements of Stictostroma gorriense Stearn. lamin. lamin. pillar mam. mam. mam. lati. spac'2/ thick. spac'g/ thick. h'ght diam. Sac g. Sac g Species 2mm* mm* 2mm mm mm mm mm cc © 6 mm Blue Fiord specimens 13-15 .04—.05 .04—.08 1 1-2 4-5 some, poor 24 S. gorriense (12-17) (.03—.06) Galloway and St. Jean (1957) 11-13 .03-.06 .02-.2 2 3-7 7-12 none 1-2 S. mamilliferum Fagerstrom (1982) 9-14 variable 1-3 as S. mamilliferum Fagerstrom 1961 as 1113 0.1 ,01-,2 (Sep 68 short 123 S. mecannelli = S. mamilliferum Parks (1936) 12 .04 .02-.16 8 none as S. mammillatum * ۲ ۲ Average spacing and range ) ( are given. Abbreviations: lamin. —laminar, spac’g—spacing, thick. —thickness, mam.—mamelon, h’ght—height, diam.—diameter, mam. spac'g mm correlation using this species and Stromatoporella per- annulata suggests that the Detroit River Group is fully Emsian in age (Prosh and Stearn, 1993). Occurrence. —Blue Fiord Formation, Ellesmere Is- land; lower member, vicinity type section (six speci- mens), lower Emsian (dehiscens Zone); upper member, Vendom Fiord (two specimens), upper Emsian (inver- sus—serotinus Zones). Stictostroma? nunavutense, new species Plate 9, figures 1-5 Diagnosis. —Thick, regularly spaced extensive lam- inae of microtubulate to ordinicellular microstructure with two to three internal tubules within thickness of lamina. Vertical elements rarely irregular post-pillars, commonly coenosteles, thick. Astrorhizal systems dif- fuse, pervasive, interrupting the lateral regularity of the structure. Description. —Skeleton hemispherical to irregular, up to 10 cm diameter; surface rough, without ma- melons or visible astrorhizae. Latilaminae crude, ir- regular, 0.5-1.0 cm thick. Vertical section: Laminae thick 0.15-0.20 mm, gent- ly undulate to irregular; variably continuous, locally interrupted by abundant foramina; spacing very reg- ular, 6 to 8 per 2 mm, specimen GSC 108876 (holo- type) average 7.0 range 6 to 8, GSC 108877 average 6.9 range 6 to 8 (each n=10). Laminar microstructure microtubulate to ordinicellular; lateral tubules com- monly 2 to 3 within the thickness of laminae, 0.02 mm wide; microstructure commonly diagenetically altered to transversely fibrous or compact. Pillars and coe- nosteles variable in form; most commonly as thick as laminae, 0.10-0.20 mm; stout, uniformly thick or slightly expanding to meet overlying lamina; randomly offset, locally superposed over three or four laminae; thin pillars fewer, rod-shaped, as thin as 0.05 mm; “-C—mamelon spacing millimeters center-to-center, lati. —latilaminar. P.40). Major morphologic measurements of previously described occurrences and of the Blue Fiord specimens AS Shown in Table 1. The Blue Fiord specimens fall Within the specific range of variation for most criteria, with the spacing of their laminae falling at the closely- Spaced extreme. Narrowly spaced laminae distinguish 5. gorriense from the closely related species S. prob- lematicum and S. anomalum (see Fagerstrom, 1982). As is apparent in Table 1, there is considerable vari- ation in morphometric ranges between described oc- Currences. Some of this variation may be due to geo- &raphic variability, but most, as noted by Fagerstrom (1982), is artifactual, due to excessively small sample izes, A feature of considerable importance is the devel- OPment of numerous, close-set mamelons. In contrast to previous descriptions, the mamelons of Blue Fiord : Sorriense are smaller and more crowded, but oth- erwise similar in terms of form and arrangement. Al- though numerous (on exposed growth surfaces), the Mamelons of Blue Fiord S. gorriense are narrow and Mostly impersistent, so that their expression in vertical hin-section is often severely muted. Development of AStrorhizae is similarly highly variable. Although Gal- loway and St. Jean (1957) diagnosed S. mamilliferum X Sorriense as without astrorhizae, Fagerstrom’s (1982) analysis of a large sampling revealed weak astrorhizae In some specimens. The same irregular development of astrorhizae occurs in the Blue Fiord specimens, "Oughly half with and half without astrorhizae. The Arctic occurrence of this species is of biostrati- Staphic significance, relating the Blue Fiord Formation i) to North American midcontinent occur- Nees of uncertain chronostratigraphy. Stictostroma Sorriense has been recorded from the lower Detroit RH Group of southern Ontario (Parks, 1936; Gal- Way and St. Jean, 1957; Fagerstrom, 1961, 1982). A | È E È BULLETIN 9 galleries occur and laminae may be discontinuous, and the skeleton itself may verge on an amalgamate struc- ture. The “background” architecture of the stroma- toporoid, as 11 were, is continuous thick laminae, dom- inantly circular galleries; the astrorhizal systems are so integrated into the skeleton, however, that this un- modified structure occurs in only about half the vertical view. All specimens of this species show variably irregular growth form, and none of the specimens is uniquely composed of this species. All show varying degrees of intergrowth with other stromatoporoid species, most commonly Gerronostroma septentrionalis n. sp. and Stictostroma gorriense Stearn, 1995. Etymology. — For Nunavut, the territory of the east- ern Canadian Arctic; in the language of the Inuit, “land of the people.” Occurrence. — Blue Fiord Formation, lower member, lower 100 m: Ellesmere Island, Eids Fiord; lower Em- sian (dehiscens Zone). Genus STROMATOPORELLA Nicholson, 1886 Type species. — Stromatoporella granulata Nichol- son, 1886 Stromatoporella perannulata Galloway and St. Jean, 1957 Plate 10, figures 1,2 Stromatoporella cellulosa Parks, 1936, .م‎ 108-110, pl. 4, figs. 6,7; non Clathrodictyon cellulosum Nicholson and Murie, 1878, p. 221, pl. 2, figs. 6-10. Stictostroma eriense Parks. Lecompte, 1951, pl. XX, figs. 2, 2a, 2b. Stromatoporella perannulata Galloway and St. Jean, 1957, p. 142- 144, pl. 9, figs. 3a,b; St. Jean, 1986, p. 1043-1045, figs. 5.4—5.6; Prosh and Stearn, 1993, Figs. 3a,3b. Stromatoporella eriensis (Parks). Galloway and St. Jean, 1957, p.145- 147, pl.10, figs. 2a,b. Stromatoporella perannulata(?) Fagerstrom, 1982, p. 38-39, pl. 7, figs. 2-4. Stromatoporella eriense(?) (Parks). Fagerstrom, 1982, .م‎ 39, pl. 7, fig. 5. Description. —Skeleton laminar, thick, only gently undulate. Surface bears few small low-relief mamelons, 0.1 mm high, 0.2 mm diameter, irregularly spaced 1> 2 cm apart, without astrorhizae; surface visibly fine granular. Latilaminae moderately to poorly developed, up to 1.0 cm thick. ۱ Vertical section: Laminae continuous, generally con- sistently parallel, rarely merging laterally, gently 0 moderately undulant; extremely crenulate on a fine- scale; very thin 0.02-0.04 mm, but commonly thick- ened and obfuscated diagenetically; regularly spaced; 7 to 10 per 2 mm, specimens GSC 108175 average 8.2 range 8 to 10, GSC 108879 average 7.7 range 7 to 8, GSC 108880 average 7.7 range 7 to 9 (all n=10); mi- microstructure of thick pillars tubulate to fibrous, of thin pillars compact. Galleries variable, commonly cir- cular 0.10-0.15 mm diameter, some laterally elongate, vermicular. Locally where interrupted by astrorhizal systems, macrostructural framework tends toward amalgamate. Dissepiments rare, very fine, 0.01 mm thick. Astrorhizae vague, indicated only by upward- doming of laminae, interruption of laminae by vertical canals, and zones of disordered lateral canals 0.15 mm diameter merging intimately with galleries. Tangential section: Thick, labyrinthine network with little open gallery space. Dominantly closed labyrin- thine network of coenosteles 0.15—0.20 mm across; isolated pillars subordinate, either subcircular dots (post-pillars) or short vermiform segments 0.10-0.15 mm diameter. Microstructure clotted, grading to ir- regularly tubulate in thick labyrinthine elements and laminae. Astrorhizae common, defined by short, branching astrorhizal paths between coenosteles, weakly ordered radial zones of short irregular canals 0.15 mm diameter, grading rapidly into labyrinthine gallery space. Astrorhizal centres spaced about 6 mm apart. Material. —Six specimens, ranging from poorly to well preserved. Holotype GSC 108876, paratypes GSC 108877 and 108878. See Appendix 3 for other speci- mens. Discussion. — Stictostroma? nunavutense n. sp. is characterized by thick, regularly spaced laminae, gen- erally egually thick pillars that are either offset or ir- regularly superposed, and tubulate microstructure. It is an unusual new species not readily assignable to known genera. Compared to most species of Sticto- stroma, the skeletal elements of S.? nunavutense are much thicker and less regularly arranged. It 1s tenta- tively assigned to Stictostroma on the basis of its con- tinuous laminae, non-superposed pillars, and similar microstructure. Numerous stromatoporellid species (of Stromatoporella, Stictostroma, and Clathrocoilona) have previously been described as microtubulate (e.g., Birkhead, 1967: Zukalová, 1971). The astrorhizae of Stictostroma? nunavutense n. sp. are unusually diffuse and apparently pervasive. They do not form discrete structures, but rather considerably modify the structural architecture of the stromatopo- roid at intervals: in this indirect way they are diag- nostic. In vertical section the astrorhizae per se are difficult to locate, defined by zones of vertically elon- gate canals that intimately merge into the gallery net- work. In tangential section they are more easily iden- tified, forming clusters of canals that again merge ra- dially into galleries. Tangential sections indicate the astrorhizae are abundant and very closely spaced (about 6 mm apart). In vertical section, therefore, the astro- rhizae may simply appear as zones where complex DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN p Group of Ontario, and from the Columbus Limestone near Marblehead, Ohio. St. Jean (1986) described S. perannulata from the Port Colborne area (Niagara Pen- insula) of Ontario, in rocks of uncertain assignment (Bois Blanc Formation or lower Onondaga Limestone). The Port Colborne specimens of St. Jean (1986) are strikingly similar to those from the Blue Fiord For- mation (compare Plate 10, figures 1 and 2 herein to figs. 5.4 to 5.6 of St. Jean, 1986). Stromatoporella eriensis (Parks) does not objectively differ from S. perannulata, and most references to S. eriensis should be transferred to S. perannulata. As noted by Fagerstrom (1982), the presumed difference, that S. perannulata has mamelons and 5. eriensis has none, 15 untenable. Larger collections of specimens (of Fagerstrom, 1982, and herein) demonstrate variable development of mamelons in S. perannulata. In given specimens mamelons may be weakly developed or lo- cally absent, and therefore present in some thin-sec- tions and absent in others. The synonymy herein in- cludes all references to Stromatoporella eriensis exclu- sive of the type specimens of Parks, 1936 (originally referred to Stictostroma eriense). Examination of Parks’ types reveals specimens unlike S. perannulata. Parks’ holotype 2610.D (ROM 13190) shows more widely spaced laminae (6 to 8 per 2 mm) that are at least twice as thick (0.05-0.10 mm) as those of S. perannulata. Also the strong crenulation of laminae into the pillars of S. perannulata is poorly developed in Parks' types (2601.D, 2602.D, 2603.D). Although assignable to Stromatoporella, Parks' types represent a species other than S. perannulata. 'The species Stromatoporella er- iensis (Parks) therefore appears to be uniquely confined to Parks’ (1936) types, but all subsequent references to S. eriensis belong to S. perannulata. In the Arctic, S. perannulata is confined to the Em- sian Blue Fiord Formation (dehiscens to inversus Zones). The presence of S. perannulata and Stictostroma gor- riense in both the Blue Fiord Formation and the De- troit River Group of Ontario suggests these units are time-correlative, i.e., the Detroit River Group is Em- sian (Prosh and Stearn, 1993). Occurrence. — Blue Fiord Formation, Ellesmere Is- land; lower member, Eids Fiord (one specimen), Sór Fiord (2 specimens), Vendom Fiord (one specimen), lower Emsian (dehiscens-gronbergi Zones); platformal dolomitic facies, Goose Fiord, Muskox Fiord (one specimen each), mid-Emsian (inversus Zone). Genus CLATHROCOILONA Yavorsky, 1931 Type species. — Clathrodocoilona abeona Y avorsky, 1951. Clathrocoilona Yavorsky, 1931, p. 1394-1395, 1407, Rossareva, 1976, p.21; Stock, 1982, .م‎ 670-673, synonymies therein. crostructure finely transversely porous or fibrous, lo- Cally altered to compact, not tripartite. Pillars either Tings or simple posts, continuous lateral count of 100 complete pillars (GSC 108175) 51% rings 49% posts; Tings extend fully to overlying lamina, central lumen 0.03-0.06 mm across, walls as laminae 0.02-0.04 mm thick; posts simple, may very gently thicken at laminae, 0.02-0.05 mm thick; no pattern of distribution rings and posts, although either may cluster 3 or 4 consec- Utive, certain interlaminar spaces may display more of One than another; never superposed, fairly consistently Offset; spaced 6 to 9 per 2 mm, specimens GSC 108175 average 7.3 range 6 to 9, GSC 108879 average 7.3 range 6 to 8, GSC 108880 average 7.4 range 6 to 9 (all n=10); Microstructure of rings transversely fibrous, continu- Ous with laminae, of posts vaguely fibrous or compact. Galleries subequally elongate-rectangular or subcir- Cular; subcircular where ring-pillars abundant, locally forming short bead-like chains; elongate galleries up to 2 mm long locally present where pillars absent. Dis- Sepiments only locally abundant, very broadly convex, thin 0.02 mm. Mamelon columns rare (present only GSC 108175), up to 1.5 cm high; one thin section (of GSC 108175) preserves short segment (2.0 mm) cen- tral astrorhizal canal, without lateral tributaries; as- trorhizae otherwise absent. One specimen (110-236) with abundant commensal corals. Tangential section: Laminae forming meandering thin bands or lines, highly scalloped (linked partial- "Ing pillars) or confluent with ring-pillars. Ring-pillars abundant, either half total pillars (GSC 108175) or fewer than half (GSC 108879, 108880); most common Within or adjacent to laminae, less commonly within Mterlaminar spaces; wall thickness 0.02-0.04 mm, Central lumen 0.04—0. 12 mm diameter; roughly 0.10- 0.12 mm apart center-to-center; microstructure trans- Versely porous or fibrous. Post pillars small, irregular dots, 0.03-0.08 mm diameter; many intergrading Shapes between ring and post pillars. Mamelon col- umns marked by sectioned laminae forming bull’s- eyes, roughly 1-2 mm apart center-to-center; no as- trorhizae. Material.—Six specimens, ranging from poorly to exceptionally well preserved. Hypotypes GSC 108175, GSC 108879, GSC 108880. Other specimens listed in Ppendix 3. Discussion. — Stromatoporella perannulata is widely 9cumented from the North American midcontinent. he type specimens of Galloway and St. Jean (1957) Ome from the Jeffersonville Limestone near Louis- Ville, Kentucky. Many more specimens are recorded mm Southern Ontario and vicinity. Fagerstrom (1 982) 3 ted many occurrences from the Formosa Reef Lime- One (Amherstburg Formation) and the Detroit River BULLETIN 349 to the subjectivity of interpreting microstructure, we retain Clathrocoilona in the Order Stromatoporellida. Clathrocoilona vexata, new species Plate 10, figures 3, 4; Plate 11, figures 1-8; Plate 12, figures 1,2 Clathrocoilona cf. C. saginata Lecompte. Stearn, 1983, p. 549, 551, figs. 5G, 5H. Diagnosis. — Skeletal elements in alternately thick and thin successive phases; very closely spaced laminae and pillars. Description. —Skeletal form variable, commonly thin encrusting, some irregular, rarely small hemispheres. Surface irregular; small mamelons abundant, astro- rhizae imperceptible. Latilaminae 2-3 mm thick. Vertical section: Alternating zones or phases of thin and thick skeletal elements (laminae and pillars). Lam- inae very irregular, undulate, discontinuous, inter- rupted by abundant foramina and coalescing laterally; sharply inflected into shallow mamelons confined to single latilamina; spaced 9 to 14 per 2 mm, holotype GSC 108881 average 10.7 range 9 to 12, paratype GSC 108882 average 13.0 range 11 to 14 (each n— 10), thick laminae 0.06—0.15 mm; thin laminae as thin as 0.02 mm; commonly thick laminae (and pillars) at base latilamina, grade to thin at top. Pillars spool-shaped, thick 0.05-0.14 mm, or thin to 0.03 mm; commonly randomly offset between successive laminae, a few su- perposed over 2 to 4 laminae; spaced 8 to 13 per 2 mm, holotype GSC 108881 average 9.3 range 8 to 11, paratype GSC 108882 average 11.4 range 9 to 13 (each n=10); locally absent. Microstructure complex, highly variable; porous/cellular, fibrous, vermiculated, or compact; pores/cellules scattered, subspherical or ver- tically elongated, 15-20 um diameter, where juxta- posed intervening microelements 5-15 um thick. As- trorhizae poorly formed; rare short irregular vertical canals 0.10 mm diameter; subcircular or ovoid foram- ina ubiquitous, 0.3-0.6 mm lateral diameter, Dissep- iments common, abundant in areas of skeletal repair; broadly convex, thin 0.01 mm. Included organisms (gastropods, brachiopods, ostracodes, worm tubes) common. Tangential section: Laminae dense meandriform bands, discontinuous. Pillars isolated dots 0.04—0. 10 mm diameter, or short thick 0.08-0.10 mm gently curved vermiform strands. In holotype (GSC 108881) about half visible area free laminae and pillars (thin element zones); remainder dense, clotted, amalgamate, little open gallery space (thick element zones). Astro- rhizae common, widely dispersed; form rare irregularly branched aggregates; main/axial canals 0.25—0.30 mm diameter, secondary canals commonly 0.08-0.15 mm Discussion. — Yavorsky's original diagnosis of the genus, based uniquely on the type Clathrocoilona abeona, stressed strictly macrostructural details, prin- cipally the abundant astrorhizal foramina, thick con- tinuous laminae, and non-superposed pillars. He char- acterized the microstructure as compact, but noted the presence of a white median line in the laminae. Sub- sequent authors placed greater emphasis on micro- structure, and differing assessments of the composition of Clathrocoilona resulted in divergent suprageneric assignments. Galloway (1957) and Galloway and St. Jean (1957) considered Clathrocoilona to be “coarsely maculate" (although with thick, tripartite laminae), and hence assigned Clathrocoilona to the Stromatoporidae. Although Lecompte (1951) did not recognize Clath- rocoilona as valid, many species he placed in Stro- matoporella were later reassigned to Clathrocoilona (Flügel and Flügel-Kahler, 1968; Kossareva, 1976). Still, Lecompte's emphasis on the tripartite laminae of these species helped influence subsequent workers to include Clathrocoilona with the Stromatoporellidae (Zukalova, 1971) or Stromatoporellida (Stearn, 1980). Most recently, Stock (1982) placed Clathrocoilona in the Stromatoporidae, interpreting its microstructure as “originally microreticulate or melanospheric, but may be altered to compact" (p. 671), and noting the com- mon occurrence of tripartite laminae. Kossareva (1976) advanced understanding of Clath- rocoilona with a redescription of the genus and a de- tailed microstructural analysis of Yavorsky's types (re- grettably unillustrated). Kossareva described the lam- inae of Clathrocoilona as composite, made up of 2 to 4 microlaminae joined by micropillars. In Kossareva's concept the multilayered laminae appear to bear 1 to 3 light median bands, in places preserving the micro- pillars and appearing cellular, elsewhere appearing continuous or hollow. Commonly the tissue is per- meated by small pores. For much of the skeleton, Kos- sareva described the elements as having a “felted ap- pearance", implying a disordered microstructural net- work, producing a tangle of microlaminae and light bands. The foregoing brief history illustrates the variety of suprageneric assignments proposed for Clathrocoilona, and how interpretation of its complex microstructure has influenced its assignment. Similarly, Clathroco- ilona vexata n. sp. (described below) demonstrates a bewildering variety of microstructures, that has prompted one of us (ECP) to interpret them as dia- genetic modifications of microreticulation (hence fa- voring assignment to Order Syringostromatida), the other author (CWS) as variability in the original skel- etal microstructure. Owing to these uncertainties, and DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 29 in C. vexata n. sp. This range (from cellular to melan- ospheric to tubulate to ordinicellular to tripartite to fibrous to compact) can be interpreted as caused by: 1) diagenetic filling of the voids that define the micro- structure, or 2) to an original broad range of secreted skeletal material, or 3) to a combination of both. Vertical sections (PI. 11, figs. 2, 3) may show ver- tically elongate or tubular voids separated by similar fine skeletal tissue that would be called micropillars by one of us (ECP). Fine horizontal elements cross these voids, but whether they are solid plates (microlaminae) or rods (microcolliculi) is uncertain. Certain states in- terpreted as diagenetic by ECP exhibit a tangled mass of tubular voids and intervening skeletal material (PI. 11, fig. 4). This is the microstructure recognized by Kossareva (1976) as “felted" (referred to as vermicu- lated herein). Further diagenetic alteration is postu- lated to result in coarsely fibrous microstructure and ultimately compact skeletal material (PI. 11, fig. 5). In another diagenetic state, the vermiculated microstruc- ture becomes “blocky” and in tangential section ap- pears to be composed of melanospheres (PI. 11, figs. 6, 7). In the opinion of CWS these myriad micro- structures may not all be derived from originally akos- moreticulate microstructure, but indicate that the skel- etal material as originally secreted may have locally been cellular or ordinicellular, locally compact or fi- brous, and locally tubulate. Very locally the laminae of this species are tripartite or ordinicellular (Pl. 11, fig. 8). In C. vexata n. sp. cellular or akosmoreticulate microstructure only de- velops in the skeletal elements thicker than 40 ۰ Only laminae of about this thickness or greater can accommodate a single row of cellules/microgalleries 20 um high. Where the slim partitions between the cellules are not preserved, the laminae appear to be tripartite. In the opinion of ECP, this local develop- ment of tripartite structure is fortuitous and a chance result of microreticular alignment, and therefore not analagous to the tripartite laminae of the Stromato- porellida. A wide range of microstructures has been ascribed to other species of Clathrocoilona. Galloway (1957) and Galloway and St. Jean (1957) described the genus as coarsely maculate with thick tripartite laminae. The tangential section of C. fibrosa (Galloway and St. Jean, 1957; pl. 22, fig. 3b) shows a porous microstructure similar to that of C. vexata n. sp. The “coarse irregular maculae” of Galloway and St. Jean are areas of altered tubulate microstructure. Kossareva’s (1976) descrip- tion of C. abeona indicates a wide range of micro- structures as noted above. Kossareva described lami- nae as cellular or joined by micropillars, apparently similar to the ordinicellular laminae of C. vexata n. diameter; tabulae present, poorly preserved. Micro- Structure porous/tubulate, vermiculated, fibrous, ir- Tegularly melanospheric, or compact; pores scattered, locally clustered, circular to oval, 10-20 um diameter, where section oblique plunge into shallow tubules. Material.—Nine specimens, four of them well pre- Served. Holotype GSC 108881, paratypes GSC 108882, 108883. Other specimens listed in Appendix 3. Discussion. —Thirty to 40 species of Clathrocoilona are previously known; the tally is imprecise because Some species are probably redundant, others misas- Signed to genera such as Stromatoporella. The char- acteristic, extreme structural variability of Clathroco- ilona species makes comparison and identification dif- ficult. Clathrocoilona vexata n. sp. is distinguished by very narrowly spaced skeletal elements, 9 to 14 lam- mae and 8 to 13 pillars per 2 mm; most Clathrocoilona Species average around 5 to 6 laminae and pillars per 2mm. Only Clathrocoilona saginata (Lecompte, 1951) (Frasnian; Belgium) displays comparable spacing, with to 14 laminae and 6 to 10 pillars per 2 mm. C. Saginata differs from C. vexata n. sp. in its more reg- ularly arranged laminae, fewer astrorhizal foramina, and much more pronounced and persistent mamelons. This new species was earlier referred to Clathrocoilona cf. C. saginata by Stearn (1983). Another distinctive feature of C. vexata n. sp. is the alternation of zones of thin versus thick skeletal ele- ments (laminae and pillars). Similar thickness alter- nation is also exhibited by Clathrocoilona solida Ya- vorsky, 1955, C. solida (Hall and Whitfield, 1873, re- described by Stock, 1984) and C. saginata (Lecompte), and to a lesser degree by C. crassitexta (Lecompte, 195 1), C. crassum (Yavorsky, 1963), C. obliterata (Le- compte, 1951), and C. spissa (Lecompte, 1951) (but Strongly present in C. spissa of Zukalová, 1971). In C. vexata n. sp. and these other species the thickness al- ternation is pronounced, yet similar variation can be found in many, if not most species of Clathrocoilona. Areas of good preservation in tangential sections of : vexata n. sp. show small circular voids 10-20 um across and distributed randomly (PI. II, fig. 1). One of us (ECP) postulates that these, among other criteria, are evidence that the microstructure is irregularly mi- Toreticulate, a microstructure described by Stock ln akosmoreticulate. The other (CWS) would ti this microstructure largely cellular, but the dis- nction between the two is mostly semantic. The voids Or pores in tangential section would then be described a the former as microgalleries and by the latter as ellules. This porous skeletal material does not appear 0 have been secreted uniformly but originally was Parated by skeletal elements of compact tissue. A Much wider range of microstructures occurs, however, BULLETIN 349 laminae; mostly randomly offset between successive laminae, locally superposed over 2 to 4 laminae; spaced variably, 5 to 8 per 2 mm average 6.3 (n=20), locally missing for lengths up to 0.1 cm; skeletal material gen- erally solid (?compact microstructure), but a few pillars appear to be hollow (as laminae), vaguely vacuolate, or as if composed of vertical fibrils. Dissepiments com- mon, not abundant, small, shallowly convex, very thin 0.01 mm, probably mostly removed by diagenesis; commonly bridging laminar foramina, towards ma- melon axes, or within anomalously large galleries. Ma- melons large, broad, vertically persistent; indicated in part by pillars crowding, thickening and becoming more strongly superposed; astrorhizal canals undefined. Mi- crostructure ambiguous (due to poor preservation), probably compact. Rare, small vacuoles may occur at pillar-lamina junctions, or at thickened regions of ex- ternal microlaminae. Tangential section: Mamelons prominent, marked by large, well-defined bull’s-eyes of concentric laminae; astrorhizae imperceptible. Laminae thick, dense, ir- regular bands with scattered vacuoles. Pillars short, thick (0.08-0.20 mm across), isolated vermiform strands or dots (mostly irregular), rarely linking or co- alescing. Microstructure apparently compact. Astro- rhizae absent. Material.—Two specimens, one partially dolomi- tized, the second severely dolomitized (Bathurst Is- land), identified as Trupetostroma sp. and represented by hypotype GSC 108884 (PI. 12, figs. 3,4). Two ad- ditional specimens, poorly preserved and identified as Trupetostroma sp.?, are questionably assigned to this species and represented by hypotype GSC 108885 (not illustrated). Discussion. — The basic concept of ۵ embraces species with thick, pronouncedly tripartite laminae, thick, spool-shaped, superposed pillars, gen- erally vacuolate microstructure, and common cyst-like dissepiments (cf. Parks, 1936; Stock, 1982). Bathurst Island Trupetostroma sp. herein departs somewhat from the norm by demonstrating poor pillar superposition and comparatively wide laminar spacing. Its mamelon development is comparatively strong, and the total absence of definable astrorhizal canals is unusual. Both dissepiments and skeletal vacuoles are comparatively few, but their scarcity may be due to diagenetic loss. Trupetostroma dominantly occurs in rocks of Give- tian to Frasnian age (e.g., Lecompte, 1952; Galloway and St. Jean, 1957; Zukalova, 1971; Stearn, 1975b). Only a few species are known from Eifelian strata (e. 9. T. spatiosum, T. cf. schelomense , T. ramulosum © Yavorsky, 1963, Kuznetsk Basin, Mamontovo Horr zon, mid-Eifelian). No definitively Lower Devonian species are previously known. Two species described by Lessovaya (1970) as T. globosum and T. magnifica, sp. Zukalova (1971) described microstructures as finely tubulate or cellular/porous; her illustrations resemble the tubulate tissue of C. vexata n. sp. Tubulate micro- structures are also noted by Stock (1982) in C. involuta Stock, 1982 and Birkhead (1967) in C. subclathrata and in species he assigned to Stromatoporella (eg., S. indubia Birkhead), which should be transferred to Clathrocoilona. The microstructure of C. vexata n. sp. suggests that the genus includes species with a very broad range of microstructures. One of us (ECP) attributes this range to diagenetic modification of an originally pervasive akosmoreticulate microstructure; the other (CWS) at- tributes it to variability in the original pattern of skel- etal secretion. In recognition of this variability (re- gardless of origin), we both of us agree that microstruc- ture should not be used as a taxonomic criterion in assigning species to Clathrocoilona. The example of the range of microstructures found in C. vexata n. sp. can be used as a guide in interpreting the variety of skeletal material that may occur in other species of this genus. The macrostructural criteria on which Clath- rocoilona is defined are fully satisfactory in assigning species. Etymology. —Latin vexata, vexacious or trouble- some; referring to the confounding structural vari- ability characteristic of species belonging to this genus. Occurrence. — Blue Fiord Formation, lower member, Ellesmere Island; vicinity type section (seven speci- mens), Vendom Fiord (two specimens); lower Emsian (dehiscens Zone). Family HERMATOSTROMATIDAE Nestor, 1964 Genus TRUPETOSTROMA Parks, 1936 Type species. — Trupetostroma warreni Parks, 1936. Trupetostroma sp. Plate 12, figures 3,4 Description. —Skeleton laminar, highly undulate. Surface not preserved, but apparently bearing large, broad mamelons. Vertical section: Laminae thick, tripartite, contin- uous, broadly undulate, consistently parallel; aggregate thickness 0.10-0.16 mm, consisting of median clear (hollow) zone 0.04-0.06 mm thick, bordered above and below by microlaminae 0.03-0.05 mm thick, ex- terior locally thickened; spaced very regularly, 5 to 6 laminae per 2 mm, average 5.5 (n=10); rarely inter- rupted by small foramina about 0.1 mm across; a few (generally thicker) laminae display third median mi- crolamina over limited lengths. Pillars commonly spool-shaped, thick 0.06-0.15 mm (commonly 0.08— 0.10 mm), spreading and thickening broadly to meet DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 31 Ferestromatopora polaris Stearn, 1983, p. 551-552, figs. SA-C, 5E; 1989, fig. 1D. Stromatopora polaris Stearn, 1990, p. 507, fig. 3.8. ?Stromatopora aff. polaris Stearn. Webby, Stearn and Zhen, 1993, p. 158, 161, figs. SF, 23A—F, 24A. Material. — Thirty-six specimens, ranging from poor to well preserved. Hypotype GSC 108886. Other spec- imens listed in Appendix 3. Discussion. — Stromatopora polaris has been previ- ously recorded in the Arctic Islands from the lower Blue Fiord Formation (Stearn, 1983) and from Upper Lochkovian reefal blocks in the Stuart Bay Formation, Bathurst Island (Stearn, 1990). The species is described in full in Stearn (1983). The new specimens of S. polaris recognized here, from the Blue Fiord and Disappointment Bay for- mations, extend the species' range through most of the Emsian Stage, up to the serotinus Zone. Specimens from the upper Eids Formation, Ellesmere Island, are lowest Emsian, possibly uppermost Pragian. The full species range in the Arctic is therefore upper Loch- kovian to upper Emsian. Specimens from the unnamed formation on Truro and Bathurst Islands (undifferentiated patulus Zone; highest Emsian/basal Eifelian), identified as Stroma- topora hensoni n. sp., are similar to S. polaris, and probably represent a descendant species. Occurrence. —Eids Formation, upper 100 m; Elles- mere Island, Sór Fiord (five specimens); lowest Emsian (dehiscens Zone), possibly uppermost Pragian. Blue Fiord Formation, lower member; Ellesmere Island, vi- cinity type section (10 specimens), Eids Fiord (nine specimens), Vendom Fiord (two specimens), Sór Fiord (one specimen); lower Emsian (dehiscens Zone). Dis- appointment Bay Formation, reefs low in formation, Truro Island (five specimens); mid-Emsian (inversus Zone). Blue Fiord Formation, upper member; Elles- mere Island, vicinity type section (four specimens); upper Emsian (serotinus Zone). Stromatopora cf. S. hupschii (Bargatzky, 1881) Plate 13, figures 1,2 cf. Caunopora hupschii Bargatzky, 1881, p. 290. cf. Stromatopora hupschii (Bargatzky). Nicholson 1886, pl. 10, figs, 8, 9; 1891, p. 176; Lecompte, 1952, p. 268, pl. 52, figs. 2, 2a, 2b; Yavorsky, 1955, p. 106, pl. 56, figs. 3, 4. Stromatopora cf. S. hupschii (Bargatzky). Galloway, 1960, p. 627- 628, pl. 74, figs. 2a, 2b; Stearn, 1983, p. 552-553, figs. 5D, SF. Description. —Skeleton domal to hemispherical, up to 15 cm diameter. Surface undulate, but without de- fined mamelons or perceptible astrorhizae. Vertical section: Thick, dominantly cassiculate structural elements; common thin latilaminae. Skeletal elements variable thickness, 0.15—0.30 mm, common- from the Bursykhirmanian Horizon (lowest Lochko- vian) of Uzbekistan, are incorrectly assigned to Tru- Detostroma; they show a definite microreticulate mi- Crostructure, and more plausibly belong to either Par- allelostroma or Coenostroma. A species quite similar to Trupetostroma sp. herein 15 Trupetostroma(?) sp. of Fagerstrom (1982), from the lower Detroit River Group, southwestern Ontario. The Arctic and Ontario species have very similar laminar ànd pillar spacings, both lack obvious astrorhizae, and m both pillar-vacuoles and dissepiments are poorly developed. Dissimilarities include stronger pillar su- Perposition in the Ontario species, and more promi- nent mamelons and thicker compound laminae in the Arctic form. For both the Arctic and Ontario species, the material presently known 15 too scarce and poor to draw firm conclusions, but from the available evidence a close relationship is plausible. The correlation of Prosh and Stearn (1993) suggests that the Detroit River Tru- Petostroma(?) sp. of Fagerstrom (1982) is Late Emsian (Probably serotinus Zone). Two additional, poorly preserved specimens from the Upper Emsian portion ofthe Blue Fiord Formation at Vendom Fiord, Ellesmere Island, are questionably Included here as Trupetostroma sp.? The Vendom Fiord Specimens display similar laminar dimensions and Spacing to the younger Bathurst Island Trupetostroma SP., but have substantially thickened pillars and, con- Sequently, very little open gallery space. In both the Bathurst Island and Vendom Fiord forms, the material IS too poor and meager to determine if the they are Conspecific variants or separate species. For biostrati- Sraphic purposes (Text-fig. 3), the Vendom Fiord oc- Currence is treated as a questionable range extension of Trupetostroma sp. down into the upper Emsian (in- Versus-serotinus Zones). Occurrence. — Northeastern Bathurst Island, un- Named limestone formation, lower 100 m; highest Em- Slan/basal Eifelian (undifferentiated patulus Zone). l'upetostroma sp.?: Vendom Fiord, Ellesmere Island, lue Fiord Formation, upper member; upper Emsian Inversus-serotinus Zones). Order STROMATOPORIDA Stearn, 1980 Family STROMATOPORIDAE Winchell, 1867 Genus STROMATOPORA Goldfuss, 1826 E^ Species. — Stromatopora concentrica Goldfuss, Stromatopora polaris (Stearn, 1983) Plate 14, figure 5 P erestr omatopora jacquesensis Galloway. Stearn and Mehrotra, 1970, P. 20, pl. 5, figs. 5, 6. BULLETIN 349 culate phases thickest/dominant; latilaminae promi- nent, thick 0.5—1.0 cm, composed of paired cassiculate plus microlaminar phases. Microlaminae thin 0.01 mm, incomplete; variably densely spaced, to as much as 10 to 15 per mm; rare to absent in cassiculate phases; generally poorly preserved. Dissepiments rare to ab- sent. Astrorhizae large, vertically persistent; axial canal 0.40-0.60 mm diameter; lateral canals turning grad- ually to horizontal, 0.20-0.30 mm diameter. Parasitic borings common. Tangential section: Meandriform bands of alternat- ing 1) thicker, darker, labyrinthine elements (cassicu- late phases), and 2) thinner, lighter-toned, diffuse struc- ture (microlaminar phases). Skeletal elements labyrin- thine to vermiform, 0.10-0.20 mm thick; microstruc- ture finely cellular; galleries vermiform to subcircular, occupy less than half total area. Astrorhizae moder- ately large, well-formed; comprise central disordered bundle of axial canals 0.20 mm diameter, extensive radial network of thicker lateral canals 0.30 mm di- ameter; center-to-center spacing roughly 1.0 cm. Material.—Three specimens, moderately well to well preserved. Holotype GSC 108890; paratypes GSC 108891 and GSC 108892. Discussion. —In terms of its structural elements, this new species is similar to Stromatopora polaris (Stearn, 1983). The size and disposition of cassiculate structural elements in both species is very similar, and in S. polaris periodic microlaminae impart banding to the skeleton in vertical section. Stromatopora hensoni n. sp. is distinguished from S. polaris by the gross af- rangement of its skeletal elements, into alternating phases of cassiculate structure (like S. polaris) and sub- ordinate phases with abundant microlaminae. Its well developed and persistent astrorhizae are also unlike S. polaris, in which astrorhizae are poorly developed. This comparison suggests that S. hensoni n. sp. is an im- mediate descendant of S. polaris. This conclusion is supported by the stratigraphic distribution of these spe cies: S. polaris is last known from the serotinus Zone (Blue Fiord Formation), and S. hensoni n. sp. appears in the succeeding undifferentiated patulus Zone. Etymology. 一 To honor Matthew Henson, Arctic ex- plorer, companion of Peary. Occurrence. — Unnamed formation; southeastern Bathurst Island (Dyke Ackland Bay) (two specimens), Truro Island (one specimen); highest Emsian/basal Ei- felian (undifferentiated patulus Zone). Genus FERESTROMATOPORA Yavorsky, 1955 Type species. —Ferestromatopora krupennikovi YA vorsky, 1955. ly 0.20 mm; specimen averages 20.6 (GSC 108887, n=20), 19.9 (GSC 108888, n=10), 20.9 (GSC 108889, n=10) mm; network dominantly cassiculate, a merging of short vertical or sub-vertical segments, rare oblique segments, and rare, slightly thicker horizontal seg- ments; short, coalescent coenosteles may occur very locally; coenostroms absent. Galleries circular to ir- regularly vermiform. Dissepiments uncommon, may be locally clustered at specific levels, or about incon- spicuous astrorhizae. Latilaminae conspicuous, 2-4 mm thick, defined by darkened elements or thin sed- iment interlayers. Microstructure coarsely cellular, cel- lules 0.02—0.04 mm diameter. Astrorhizae inconspic- uous. Tangential section: Skeletal elements form tightly- closed, amalgamate network; element thickness 0.15- 0.25 mm, commonly 0.20 mm; microstructure cellu- lar. Galleries labyrinthine, slightly thinner than ele- ments; rarely circular to sub-circular. Astrorhizae rare, ill-defined clusters of short canal segments, 0.30-0.40 mm diameter. Material.—Six specimens, moderately well pre- served. Hypotypes GSC 108887 to 108889. Discussion. —The systematic assignment of this spe- cies is unchanged from that of Stearn (1983), despite the additional six specimens from the Blue Fiord and Eids Formations. The species Stromatopora hupschii remains no more than a convenient receptacle for spec- imens such as these, with thick structural elements but few other distinguishing features. Occurrence. —Eids Formation, upper 100 m, Elles- mere Island, Sôr Fiord (one specimen); lowest Emsian (dehiscens Zone), possibly uppermost Pragian. Blue Fiord Formation, lower member, Ellesmere Island; Eids Fiord (four specimens), Vendom Fiord (one specimen), lower Emsian (dehiscens Zone). Stromatopora hensoni, new species Plate 13, figures 3-5 Diagnosis. — Conspicuously latilaminate, alternating phases of dominantly cassiculate structure and phases with abundant microlaminae; abundant, vertically per- sistent astrorhizae. Description. —Skeleton domical, up to 15 cm di- ameter; surface smooth. Vertical section: Skeletal elements cassiculate; thick- ness variable 0.10-0.25 mm, commonly 0.15 mm, ho- lotype GSC 108890 average 0.16 range 0.10—0.25 (n=20); microstructure finely cellular. Galleries cir- cular to vermiform, 0.10-0.25 mm diameter. Alter- nating phases of cassiculate versus microlaminar struc- ture, subequally thick 3-5 mm, but commonly cassi- DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 33 differ considerably from the type description, having somewhat wider canals, little discernable pattern, and no evident vertical component. Of the few valid species of Ferestromatopora known (Stearn, 1993), all are Middle Devonian. F. krupen- nikovi, the type species of the genus, comes from the Givetian of the Kuznetsk Basin, Russia (Yavorsky, 1955). Therefore the Blue Fiord occurrence consider- ably extends the range of the genus to the lower Emsian. Occurrence.—Ellesmere Island, Eids Fiord; Blue Fiord Formation, lower member; lowest Emsian (de- hiscens Zone). Genus GLYPTOSTROMOIDES Stearn, 1983 Type species. — Glyptostroma simplex Yang and Dong, 1979. Glyptostromoides simplex (Yang and Dong, 1979) Plate 14, figures 3, 4 Glyptostroma simplex Yang and Dong, 1979, p. 66, pl. 36, figs. GC Glyptostromoides simplex (Yang and Dong). Stearn, 1983, p. 553, 555, figs. 6A-6C. Discussion. —The Blue Fiord Formation occurrence of this species has been described by Stearn (1983). Blue Fiord Glyptostromoides simplex displays a wide range of morphologies, as noted by Stearn (1983). Mor- phological variables include areas of cassiculate versus coenostromal structure, considerable variation in spac- ing of thick coenosteles, and abundance of dissepi- ments. The eleven specimens of G. simplex referred to by Stearn (1983) came from strata low in the Blue Fiord Formation, in the vicinity of the type section. These strata are now regarded as lowest Emsian (dehiscens Zone) (Uyeno, 1990). Addition of the specimens con- sidered here extends the range of Arctic G. simplex up to the serotinus Zone (upper Emsian). Material.—Twelve specimens, moderately well to poorly preserved. Hypotypes GSC 108894, 108895. Other specimens listed in Appendix 3. Occurrence. —Eids Formation, near formation top, Ellesmere Island, Eids Fiord (two specimens); lower Emsian (dehiscens Zone). Blue Fiord Formation, lower member, Ellesmere Island; vicinity type section (seven specimens), Eids Fiord (one specimen); lower Emsian (dehiscens Zone). Blue Fiord Formation, high in upper member; Ellesmere Island, vicinity type section; upper Emsian (serotinus Zone) (one specimen). Blue Fiord Formation, upper member, Vendom Fiord (Ellesmere Island), upper Emsian (inversus + serotinus Zones) (one specimen). Ferestromatopora cf. F. krupennikovi Yavorsky, 1955 Plate 14, figures 1,2 cf. Ferestromatopora krupennikovi Yavorsky, 1955, p. 109-110, pl. LVIII, figs. 1-5; Yang and Dong, 1979, .م‎ 58, pl. 28, figs. 1, 2. non Ferestromatopora krupennikovi Yavorsky. Fischbuch, 1969, p. > 176-177, pl. IX, figs. 1-5. ?Ferestromatopora krupennikovi Yavorsky. Khromych, 1974, p. 52, pl. XIII, figs. 2a, 2b. Description. —Skeleton domal, up to 8 cm diameter. Growth surfaces irregular, but without noticeable ma- Melons, Vertical section: A highly irregular network of ver- tical-to-inclined elements and dissepiments, bounded by paralaminae. Paralaminae mostly continuous, un- dulate, thin 0.03-0.04 mm; spaced irregularly 0.3-1.4 Mm apart, commonly 0.6-0.8 mm apart. Interlaminar Network chaotic, consisting of short, vertical or in- clined elements, 0.06-0.08 mm thick, merging with or bridged by abundant, convex dissepiments, 0.01-0.02 mm thick; where vertical elements abundant, spaced Toughly 10 per 2 mm. Microstructure indeterminate. Galleries commonly squarish, arch-roofed, or irregular Or sub-round; well-formed galleries 0.25-0.40 mm lat- Cral diameter; galleries generally randomly offset, but immediately adjacent to paralaminae may align lat- sh ally. Basal layers thin, composed of stringy, sinuous, discontinuous vertical elements, and discontinuous Paralaminae. Astrorhizae obscure; vertical systems im- Per ceptible; lateral canals roughly 0.30 mm wide; dis- Sepiments large and abundant within astrorhizae. Tangential section: A tightly linked, cassiculate net- tee elements 0.03-0.06 mm thick, only rarely as Olated dots 0.03 mm diameter. Microstructure Vaguely cellular. Paralaminae form thin, meandering ands, weak concentric arrangement. Astrorhizal ca- “ia numerous, appear as short, straight or simply i anched segments, 0.20-0.35 mm wide; canals clus- ered, but otherwise without definable pattern. Material. —One specimen, preservation mediocre. Hypotype GSC 108893. Discussion. — This Blue Fiord specimen resembles Bas estromatopora krupennikovi Yavorsky, 1955 in a 5 of ways. Its cassiculate structural elements are ar In size and arrangement, and the wide range of لج‎ of paralaminae is identical. In the original de- ption of the species, Yavorsky (1955) emphasized © cellular shape of the galleries, and characterized Kb arrangement relative to each other as “chess-like CT“, in other words alternately offset. In contrast, © galleries of the Blue Fiord specimen are more ran- py arrayed, and a bit larger than in F. krupennikovi. * astrorhizal systems of the Blue Fiord specimen BULLETIN 349 which both occur in the lower Emsian portion of the Blue Fiord Formation. In vertical section, the coeno- steles of Salairella prima are generally thinner and more vertically coalescent, but a few specimens of S. prima have coenosteles approaching the condition of Syringostromella zintchenkovi, and if dissepiments are unusually abundant, the species may be difficult to distinguish. Ultimately, Syringostromella and Salai- rella must be discriminated in tangential section, Syringostromella forms a tight labyrinthine network, and in Salairella round coenotubes predominate. Blue Fiord Syringostromella zintchenkovi is similar to Syringostromella labyrinthea Stearn, 1990 from Lochkovian reefal blocks on Bathurst Island (Stearn, 1990). In S. labyrinthea, however, the coenosteles are thinner and more closely spaced. Stearn (1990) syn- onomized S. labyrinthea and S. cf. zintchenkovi tenuis Khalfina, 1961 of Khromych (1976), a form found in the Emsian of eastern Siberia. S. zintchenkovi tenuis itself was established by Khalfina (1961), for specimens younger than S. zintchenkovi s.s, from the Maloba- chatski horizon (Pragian, overlies the Krekovski ho- rizon), and with thinner and more closely spaced coe- nosteles than S. zintchenkovi. It therefore appears that in the arctic Lower Devonian, older Syringostromella has the thinner elements, and in Siberia the opposite occurs, with thinner elements in younger forms of Syr- ingostromella. As such, this Syringostromella zintch- enkovi-labyrinthea assemblage of species is of dubious biostratigraphic value. Syringostromella zintchenkovi has also recently been recognized from the lower Pragian Lilydale Limestone of Victoria, Australia (Webby et al., 1993). Occurrence. —Blue Fiord Formation, lower mem- ber; Ellesmere Island, formation type area (one spec imen), Sór Fiord (one specimen); lower Emsian (de- hiscens Zone). Genus SALAIRELLA Khalfina, 1961 Type species. —Salairella multicea Khalfina, 1961. Salairella prima Khromych, 1971 Plate 15, figures 4, 5; Plate 16, figures 1—5 Salairella prima Khromych, 1971, p. 132, pl. 36, figs. la, 10: ۰ 1983, p. 555—556, figs. 6D-6G; Webby and Zhen, 1993, p. 342, 344, figs. 9C—E, 12A, B. Material. — Twenty-nine specimens. Hypotypes GSC 108898 to 108901. Other specimens listed in Appendi* 3. Poor to exceptionally well preserved. Discussion. — The Blue Fiord Formation occurrence of this species is described by Stearn (1983). The new specimens of Salairella prima recognize! herein allow for some broadening of the concept of this species. Of the 29 specimens assigned to S. prima, 2 Family SYRINGOSTROMELLIDAE Stearn, 1980 Genus SYRINGOSTROMELLA Nestor, 1966 Type species.— Stromatopora borealis Nicholson, 1891. Syringostromella zintchenkovi (Khalfina, 1961) Plate 15, figures 1-3 Stromatopora aff. hupschii (Bargatzky). Ripper, 1937a, p. 186, pl. 8, figs. 7-8. Stromatopora zintchenkovi Khalfina, 1960, p. 327—328, pl. D-3, figs. la, 1b. Syringostromella zintchenkovi (Khalfina). Webby, Stearn and Zhen, 1993, p. 163, figs. 23E-F, 24A-C. Description. —Skeleton laminar, thick; up to 15 cm lateral diameter. Surface not preserved. Vertical section: Thick, persistent coenosteles, abun- dant dissepiments. Coenosteles vertically persistent, parallel to one another, straight or gently sinuous; may branch and coalesce vertically, but not commonly; thick, 0.20-0.40 mm, GSC 108896 range 0.21-0.35 mm average 0.27 mm (n=20), GSC 108897 range 0.20- 0.40 mm average 0.27 mm (n=20); spacing 3 to 6 per 2 mm, commonly 4 to 5 per 2 mm, GSC 108896 range 3 to 4 average 3.8 per 2 mm (n=10), GSC 108897 range 4 to 6 average 4.7 per 2 mm (n=10). Short coe- nostromal segments locally present, up to 0.5 cm long, 0.25-0.30 mm thick. Dissepiments very abundant, thin, 0.02 mm; horizontal to gently convex, commonly spanning vertical galleries between coenosteles, but lo- cally up to 0.5 mm long; commonly aligned laterally; vertical spacing 5 to 8 per mm. Microstructure finely cellular. Astrorhizae inconspicuous. Tangential section: Coenosteles form tightly linked, labyrinthine network; galleries sausage-shaped rarely subcircular. Coenosteles 0.20-0.40 mm thick; micro- structure finely cellular. Astrorhizae inconspicuous, evident only as short canal segments, 0.30 mm wide. Material. — Two specimens. Hypotypes GSC 108896, 108897. Moderately well preserved. Discussion. — Syringostromella zintchenkovi (Khal- fina, 1961) is previously known from the Salair of south- central Russia, Krekovski horizon (upper Lochkovi- an) The Blue Fiord Formation specimens conform very closely to the original description of Khalfina (1961): coenosteles 0.17-0.32 mm, commonly 0.21— 0.29 mm thick, rarely thicker, spacing 2 to 3 per mm. Khalfina (1961) characterized the “zooidal tubes" (in- tercoenostele galleries) as somewhat narrower than the coenosteles themselves, the same condition as in the Blue Fiord specimens. Although Khalfina (1961) gave ° dimensions for the astrorhizae, they are described as small and poorly-defined, in the Blue Fiord specimens astrorhizae are scarcely apparent. Syringostromella zintchenkovi may be confused with certain specimens of Salairella prima Khromych, 1971, DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 35 distant from that of the Stromatoporida. The species appears to show both microreticulate and cellular mi- crostructure. If microstructure is taken as the sole cri- terion of membership in the Syringostromatida and the species is dominantly microreticulate, then S. pri- ma should be transferred to the genus Parallelopora Bargatzky within this order. The ambiguity of the microstructure of S. prima is made no clearer when specimens are viewed in tan- gential section (PI. 16, figs. 3,4). Stearn (1993) has sug- gested that microreticulate and cellular microstructure may be discriminated when viewed in tangential sec- tion, by noting the character of microelements at the edge of skeletal (macro)galleries. Coenosteles with pro- truding microcolliculi at gallery edges should produce a ragged boundary; in contrast, coenosteles of cellular microstructure should have smooth gallery edges. Un- fortunately such ragged edges may be easily corroded in diagenesis. Specimens of Salairella prima exhibit both these features in tangential section (PI. 16, figs. 3,4), implying the genuine coexistence of both mi- crostructures. Detailed assessment of the classification of the Stro- matoporida and the position of Salairella prima in it is beyond the scope of this study. If S. prima can be shown to be basically more microreticulate than cel- lular, then it should be transferred to a genus within the Syringostromatida. If, on the other hand, the sug- gestion of microreticulation is the result of occasional superposition of cellules (rather than a basic post-and- beam microarchitecture) then it can be retained within the Stromatoporida. Occurrence. —Eids Formation, upper 100 m; Elles- mere Island, Eids Fiord (one specimen), Sör Fiord (five specimens); lower Emsian (dehiscens Zone), possibly uppermost Pragian. Blue Fiord Formation, Ellesmere Island; lower member, lower 150 m; vicinity type sec- tion (10 specimens); Eids Fiord (five specimens); Sor Fiord (two specimens); Vendom Fiord (three speci- mens); lower Emsian (dehiscens Zone). Disappoint- ment Bay Formation, reefs near base of formation; Truro Island (one specimen), Lowther Island (one specimen); mid-Emsian (inversus Zone). Blue Fiord Formation, upper member, near top; Ellesmere Island, vicinity type section; upper Emsian (serotinus Zone) (one specimen). Order SYRINGOSTROMATIDA Bogoyavlenskaya, 1969 Family SYRINGOSTROMATIDAE Lecompte, 1951 Genus ATOPOSTROMA Yang and Dong, 1979 Type species.—Atopostroma tuntouense Yang and Dong. 1979. of them conform to the description of Stearn (1983). Four of the new specimens exhibit a greater abundance of dissepiments, but in all other features conform to the earlier description (Stearn, 1983). In vertical sec- tion (PI. 16, fig. 1), the abundant dissepiments are ar- ranged like tabulae, ascending the vertical galleries be- tween the coenosteles. The dissepiments are small and Very thin, so that in many specimens their scarcity may be due in some degree to diagenetic removal. As noted by Stearn (1983), the majority of specimens Of S. prima demonstrates only obscure and inconspic- uous astrorhizae. Two of the new specimens, however, exhibit well formed, although widely scattered astro- rhizae (Pl. 16, fig. 2). In these rare specimens the as- trorhizae form radiating lateral branches 0.20-0.25 mm across. Specimens of S. prima in the original collection of Stearn (1983) came from low in the Blue Fiord For- Mation, in lower Emsian strata (dehiscens Zone). The New specimens extend the species’ range in the Arctic UP to the upper Emsian (serotinus Zone). The type of S. prima is from the Neludimskaya suite in the Omu- levski Range of Severo-Vostok, eastern Siberia (Khro- mych, 1971). Although Khromych (1971) indicated the age of these rocks as Middle Devonian (reiterated m Stearn, 1983), in a later publication (Khromych, 1976) the Neludimskaya suite is shown to be Early *vonian (probably Pragian) in age. S. prima has re- cently been described (Webby and Zhen, 1993) from © Jesse Limestone, New South Wales, Australia, Where it is Emsian, probably early Emsian age. A few of the new specimens of S. prima preserve Microstructure in very fine detail (Pl. 16, figs. 3—5). For * most part, the microstructure of S. prima is finely Cellular (e.g. Pl. 16, fig. 3). In some specimens (most wam GSC 108898, PI. 16, fig. 5), however, the “cel- i es are strongly aligned at certain levels, such that © microstructure becomes orthoreticulate. Stearn 1989) made a similar observation, noting the micro- Ucture of S. prima as cellular with local traces of sp roreticulation. Webby and Zhen (1993) have also it died the microstructure of S. prima, suggesting that JS probably microreticulate rather than cellular. The ausn between skeletal tissue in which the cellules ned vertically and that in which micropillars microcolliculi define the microarchitecture is a me one. In the recent phylogeny of the Stromato- És Ida proposed by Stearn (1993) microreticulate gen- E are grouped in the Order Syringostromatida and » ular genera are placed in the Stromatoporida. Sa- Vella is placed here in the Stromatoporida because gu Microstructure of most of its species is dominantly ular. If Salairella prima is interpreted as typically JeToreticulate, then its ancestry would be interpreted Y Stearn (1993) as within the Syringostromatida and BULLETIN 349 cal, up to 10 cm diameter. Growth surfaces with barely perceptible mamelons of very low relief, astrorhizae present. Vertical section: Structure a network of microlam- inae and much thicker, diffuse pillars. Microlaminae continuous, very gently undulate, may coalesce later- ally; 0.01—0.03 mm thick; readily obscured by diagen- esis, may locally appear as a chain of fine dots or beads; spacing variable, 10 to 20 per 2 mm, average 14.6 (n=11). Latilamination irregular, marked by dark per- ithecal layers following growth interruption, thickness very variable, 2 mm to 2 cm. Pillars stout, 0.10-0.15 mm thick; mostly column-like, or may expand gently upward to coalesce at overlying microlamina, forming coenostroms; mostly vertical, some gently inclined; commonly confined to interlaminar space, irregularly offset, less than half total pillars superposed over two coenostroms, rarely superposed over 3 to 4; spaced 7 to 11 per 2 mm, average 8.4 (n=17). Pillar microstruc- ture orthoreticular to clinoreticular, but preservation generally poor. Galleries commonly circular or oval (long-axis horizontal), mostly 0.2-0.3 mm across, rare- ly horizontally elongate to 0.5 mm or more. Astrorh izal systems well developed, large and vertically persistent, no axial canal, lateral canals 0.15-0.20 mm wide; in- clined tabulae common along lateral branches, other- wise absent in skeleton. Tangential section: A tangled, irregular network ex- hibiting very little open gallery space. Laminae (coe- nostroms) thick, diffuse, concentric bands. Microlam- inae imperceptible. Pillars form irregular, intercon- nected chains, 0.10-0.15 mm thick; only very rarely as isolated irregular dots between laminae. Microstruc- ture cellular (=irregular microreticular). 6م‎ conspicuous, common; canals 0.20—0.25 mm diame- ter; comprised of about 8 to 10 radiating lateral canals, no axial canal; center-to-center distance fairly consis- tent, about 6 mm; present at mamelon summits, but not confined to them. Material. — Seventeen specimens, moderately well to poorly preserved. Hypotypes GSC 108903 to 108905. Other specimens listed in Appendix 3. Discussion. — Habrostroma proxilaminatum is pre” viously known from the Devonian of southwester? Ontario (Fagerstrom, 1961, 1982), and the Arctic spec imens differ very little from Fagerstrom's descriptions Fagerstrom (1982) distinguished H. proxilaminatu™ from two similar species (H. densilaminatum and H. formosense) primarily on the basis of microlaminať spacing, recognizing a continuum of variation between the three species, with H. proxilaminatum interme" diate in position, having microlaminar spacing on the order of 15 to 22 per 2 mm. The spacing of the ۴ specimens falls slightly lower (10 to 20 per 2 mm Atopostroma distans (Ripper, 1937b) Plate 18, figure 5 Actinostroma stellulatum var. distans Ripper, 1937b, p. 12, pl. 2, figs.1,2. Trupetostroma cf. T. ideale Birkhead. Stearn and Mehrotra, 1970, p. 16-17, pl. 5, figs. 1, 2. Atopostroma tuntouense Yang and Dong. Stearn, 1983, p. 548-549, figs. 4E-H. Atopostroma distans (Ripper). Webby and Zhen, 1993, p. 346-348; figs. 11A-D, 12E, Webby, Stearn and Zhen, 1993, p. 171, 173, figs. 27F, 28A-D. Material. — Four specimens. Hypotype GSC 108902. Preservation mediocre to moderately well preserved. Discussion. — The Blue Fiord Formation occurrence of this species has been previously described by Stearn (1983) as Atopostroma tuntouense Yang and Dong, 1979. The four specimens of Atopostroma distans re- corded here, including one from the Bird Fiord For- mation, display the following measurements: laminar spacing 7 to 11 per 2 mm (averages n=10 each spec- imen: 8.4, 8.4, 9.5, 9.9); pillar spacing 8 to 10 per 2 mm (averages n—10 each specimen: 9.2, 8.6, 8.7, 9.0); laminar thickness 0.02-0.04 mm; pillar thickness 0.08— 0.10 mm. Blue Fiord specimens earlier assigned to Atopostro- ma tuntouense by Stearn (1983) have been referred to Atopostroma distans (Ripper) (Webby and Zhen, 1993). In Australia, A. distansis known from the Emsian Jesse Limestone, New South Wales (Webby and Zhen, 1993), and from the Buchan's Cave Limestone, Victoria (bas- al Emsian) (Webby et al., 1993). As noted in Webby and Zhen (1993) and Webby et al. (1993), specimens referred to Atopostroma tuntouense from the upper Lochkovian Stuart Bay Formation of Bathurst Island (Stearn, 1990) are not conspecific with Blue Fiord spec- imens. Occurrence. — Blue Fiord Formation, lower member, Ellesmere Island; Eids Fiord (two specimens), vicinity formation type section (one specimen); lower Emsian (dehiscens Zone). Bird Fiord Formation, near forma- tion base; Ellesmere Island, Bird Fiord (near type lo- cality) (one specimen); uppermost Emsian/basal Eife- lian (undifferentiated patulus Zone). Genus HABROSTROMA Fagerstrom, 1982 Type species. — Stromatopora proxilaminata Fager- strom, 1961. Habrostroma proxilaminatum (Fagerstrom, 1961) Plate 17, figures 1—5 Stromatopora proxilaminata Fagerstrom, 1961, p. 8, pl. 1, figs. 4-6. Habrostroma proxilaminata (Fagerstrom). Fagerstrom, 1982, p. 13- 15, pL 1,1198. 7, 8. Description. —Skeleton hemispherical to subspheri- DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 37 Island, Dyke Ackland Bay; unnamed limestone for- mation, lower 100 m; highest Emsian/basal Eifelian (undifferentiated patulus Zone) (two specimens). Genus PARALLELOPORA Bargatzky, 1881 Type species. — Parallelopora ostiolata Bargatzky, 1881. Parallelopora campbelli Galloway and St. Jean, 1957 Plate 18, figures 1-4 Parallelopora campbelli Galloway and St. Jean, 1957, p. 208-210, pl. 19, figs. 3a, b. Description. —Skeleton tabular, up to 10 cm diam- eter. Growth surface undulating, but without defined mamelons. Vertical section: An irregular network of branching and anastomosing coenosteles, with only short, dis- continuous coenostroms. Coenosteles 0.05—0.15 mm thick, most commonly 0.10 mm thick; mostly verti- cally aligned, continuous over 1 to 4 coenostromal bands, or branching and coalescing; locally in small areas of irregular network vertical fabric is suppressed; spacing regular, 7 to 10 per 2 mm; specimen GSC 110314, 7 to 10 per 2 mm average 8.3 (n=20); spec- imen GSC 110315, 7 to 9 per 2 mm average 7.7 (n=10); specimen GSC 110316, 7 to 10 per 2 mm average 8.4 (n=10). Coenostele microstructure orthoreticulate, mi- crogalleries 0.04 mm diameter. Horizontal fabric sup- pressed; locally coenosteles may merge laterally to pro- duce short coenostromal segments about 5 mm long, 0.10-0.20 mm thick; where partial coenostroms occur in sequence, spacing roughly 6 to 8 per 2 mm. Dis- sepiments present, not abundant; common within and adjacent to astrorhizae; elsewhere dissepiments very flat, joining laterally over short lengths locally sug- gesting microlaminae. Latilaminae absent, although 3 to 5 mm thick bands of strongly aligned coenosteles alternating with cassiculate network suggest growth pe- riodicity. Galleries subequally vertically elongate, roughly 0.15 mm wide by 0.30-0.40 mm long, or round, 0.15-0.25 mm diameter. Astrorhizae irregular, verti- cally persistent; canals wide, 0.25-0.40 mm; unasso- ciated with any structural deflection within skeleton. Tangential section: A dense network with little open gallery space. Horizontal fabric imperceptible, little suggestion of concentric banding apparent. Coeno- steles chainlike, joined, not separate; thickness highly variable, 0.05-0.25 mm, commonly 0.10 mm, locally fused into thick clumps; occuping over half total area. Microgalleries 0.04 mm diameter. Galleries either short vermiform areas, 0.10 mm wide, or round coenotubes 0.10 mm diameter. Astrorhizae common; inconsis- average 14.6), thus approaching the field of H. densi- laminatum. The poorer preservation of the Arctic Specimens suggests some diagenetic loss of microlam- Mae, biasing the measurements towards artificially low values. Fagerstrom's (1961) original description of the Species cites a wider pillar spacing (2 to 3 per 1 mm), but his photographs (1961, 1982) demonstrate pillar Spacing comparable to that of the arctic specimens. In all other significant features the arctic and southern Ontario specimens are identical: pillar thickness and arrangement; gallery shape, size, and disposition; as- trorhizal size, abundance, spacing, lack of axial canal, and exclusivity of tabulae. In the Devonian of Ontario, H. proxilaminatum is long-ranging, occurring in the Detroit River Group through the upper Dundee Formation, and possibly in the underlying Bois Blanc Formation (Fagerstrom, 1982). In the Arctic, H. proxilaminatum is known to Occur at two localities, in the lower Disappointment 'ay Formation on Truro Island, in strata of mid-Em- Slan age, and in the lower unnamed formation on Bath- Urst Island, in strata spanning the Emsian-Eifelian oundary. Its observed range in the Arctic is therefore from the inversus Zone through the undifferentiated Patulus Zone (Text-figure 3). The Arctic occurrence of : Proxilaminatum further strengthens the Blue Fiord- to-Detroit River correlation of Prosh and Stearn (1993), m which common stromatoporellid species are inter- pr eted to give an inversus-age for the Bois Blanc For- mation, and a serotinus-age for much of the Detroit 1 00 Group. By this correlation, the inversus—patulus nge of Arctic H. proxilaminatum corresponds to the پم‎ Blanc through Detroit River interval of its range i ntario. Also, the addition of H. proxilaminatum > the correlation indicates that a major migration of retic stromatoporoids to the midcontinent took place uring late Emsian time. Oddly, H. proxilaminatum is absent from our large Fiord Formation collections, yet at Truro Island * of the specimens collected are H. proxilami- um. That this is no sampling artifact is show by the arge discrepancy in abundance of samples. It is inter- Preted to indicate a clear environmental preference. © depositional setting of Truro Island is quite unlike © large, shelf-margin reefs of the type Blue Fiord on ioe Island; rather, very small reef knolls in a ap Ticted, platformal setting are indicated for the Dis- ent Bay Formation on Truro Island. Fager- m (1961) noted that H. proxilaminatum is the most Undant stromatoporoid species in the Formosa reefs OWer Detroit River Group) of southern Ontario. Occurrence. —Truro Island; Disappointment Bay ormation, small reef knolls near base of formation; Mid-Emsian (inversus Zone) (15 specimens). Bathurst | 38 BULLETIN 349 but on the basis of regional stratigraphy (Prosh and Stearn, 1993), believed most probably to be of patulus- age. The foregoing suggests that the Arctic and midwest specimens are of identical age, but too much uncer- tainty remains concerning their respective stratigraph- ic ranges. It is also quite possible that the range of Arctic P. campbelli extends down into the serotinus Zone; the Blue Fiord Formation at this level is dolo- mitic and poorly fossiliferous, and we have few stro- matoporoids collected from this interval. Occurrence. — Bathurst Island, Dyke Ackland Bay, unnamed formation, lower 100 m; highest Emsian/ basal Eifelian (undifferentiated patulus Zone). Appendix 1.—Collection localities. Num- ber on text- fig. 1 location of sections* latitude N longitude W 1 AD Sale uk 86?49'31" p AA qaippe 86%46'26" 3 AB Te a 86%41"11" 4 AC TITI ya 8623626" 5 BC TTP 14/21" 86?19'3" 6 CA Hrs REM S: 85245'28" Vë CH TI LIU 83951 I2 8 els LDA 8547'9" 9 CD بای‎ Ae 85°47'37" 10 CE 77014'28" 859120 11 CH SLOTS 8520 12 IA 77°16'59” 86°1'26" 13 IB JAA ode hk JA 14 IC ALO 86% 8“ 15 ID TIL 85057'9" 16 Castle bioherm 77°16'0” 85245'0" 17 EA TII DOE 85°7'8" 18 EC TE I ek 8599/31" 19 K Sl (RZ cu 8528" 34" 20 Bird Fiord Type isis ett nj 86°35'20" 21 (no section) TTO O 85°54'0" 22 ED 77°29'41" 835417" 29 U-9 e RU UD 8636'26" 24 FA 1123621957 88%29"3" 242 KB 10202136" 87°38'48" 26 GA 77°44'28" 83°29'3” Zi GB 77%42'42" 83%30'0" 28 HA OSS 8342/23" 29 HB ge OD” 83.486" 30 Loc. 43 Tal owe 83045'43" 31 Vendom 1 77939'45" 83°31'0" SZ Vendom 4 JI O E 83945'93" 33 Lowther Island 74°33'30" 97929'30" 34 Truro Island 75923'45" 9721310" 35 B22 (Bathurst I.) 76°29'14” 98°14'42" 36 B42A (Bathurst I.) St KE Ab 99°8'37" + Letters (e.g., AD) designate measured sections in Smith (1984). tently formed, may consist of a loose central bundle of a few axial canals, surrounded by 3 to 6 irregular radiating lateral canals; lateral canal width variable, 0.20-0.30 mm; center-to-center spacing 5-8 mm. Material.—Five specimens, moderately well pre- served. Hypotypes GSC 110314 to 110316. Discussion. —Parallelopora campbelli is previously known from the Devonian of Indiana and Ohio (Gal- loway and St. Jean, 1957). It is, unfortunately, known from only a few specimens, and Galloway and St. Jean’s description is based on the unique holotype. Despite this, the Arctic specimens are identical to Galloway and St. Jean’s description in every significant regard. Pillar thickness and spacing are identical in both the Arctic specimens and the holotype, and they have com- parable microstructure. The discontinuous coeno- stroms of the Arctic specimens compare to what Gal- loway and St. Jean (1957, p. 209) described as “vari- able and discontinuous” laminae, and thicknesses and spacings are the same. Similarly, Galloway and St. Jean (1957, p. 209) noted “discontinuous microlaminae and curved plates”, described as dissepiments herein. In tangential section, the holotype and Arctic specimens show the same subequal distribution of vermicular and round galleries (= coenotubes). Of particular note are the odd astrorhizae and complete lack of mamelons. In their systematic description of the species, Gal- loway and St. Jean (1957, p. 210) mentioned the oc- currence of only the holotype, from the Jeffersonville Limestone near Kent, Indiana. Elsewhere (p. 80) they noted its rare occurrence in the “Columbus limestone”’ at Kelleys Island, Ohio. This latter mention is impor- tant, because it permits a more precise appraisal of the age of P campbelli. In a detailed study of the stro- matoporoids of Kelleys Island, Bjerstedt and Feld- mann (1985) indicated that Galloway and St. Jean’s “Columbus” stromatoporoids in fact come from the upper Lucas Formation (Detroit River Group). P. campbelli is not recorded in Fagerstrom’s (1982) large Detroit River Group collections. P. campbelli therefore constitutes another element in a major exchange of stromatoporoid species between the Arctic and the midcontinent during the late Em- sian. The limited occurrence of P. campbelli in both the Arctic and midwest precludes precise correlation, but the ages of these known occurrences are closely comparable. Following from the stromatoporellid- based correlation of Prosh and Stearn (1993), the upper Lucas Formation is either of serotinus or more prob- ably patulus Zone assignment. The Arctic specimens come from one locality dated as undifferentiated pa- tulus Zone (patulus + partitus Zones; cf. Text-fig. 3), 29 DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN Appendix 2.— Catalogue of type numbers and locations of type specimens. Specimens in type collection of the Geological Survey of Canada, long. west 86°49'31” 85?47'9" 85°47'9" 919115307 99%8'37" 9998'37" 83°30'0" 85%45'28" NC 83293” 864111” 86°36'26” 83230'0" 5929 94. 8829˙3“ 83°31'0" 87°38'48" 9891442" 98921442" 9891442" 9891442" 862195. 869193. 85251'12" 85°47'9" 85%47'9" 86°41'11" 86°41'11" 8693626" 8673626" ا لا وه‎ SI لا‎ SI 86°41'11" 86*46'26" 8641711" 9891442" 8393170" 97:13 10" 86°41'11" 86°46'26" 86941"11" 971130 55557 992837" 86%46'26" 83°31'0” 8619 5. Soo al. 5 0002901. 859834" 834543" 86%46'26" 86°46'26" 97*13'10" 97°13'10” 971310? IOI 9998137" 99831" lat. north SR TILDA VALORI 75°17'0” VALE de ps pes اح‎ SE 77%42'42" sa] LA Bs EN M 77°44'28" 7 E. 711936" 77%42'42" CIS 76%36'19" 77%39'45" 16°3 136" 76%29"14" 76%29"14" 76%29"14" 76?29'14" 77°14'21" 77e14˙21“ 7 Ue T4621 Ta ELA 77202” (10200 2 TENSO 11:19 90. TTY7'34" 77°17'34" TAU 73-20 2 71:202" 76°29'14" 77°39'45" 75°23'45" 110202" 712002" TIMO 1 1/0: 105351: 73 905 77°20'2" 77°39'45" 771421" 71734" “EM TY Ey" VVT A. 1102130" T1204" 71202" 75?23'45" 75?23'45" 7592343" ia ole TOSE 73 loca- tion 0 — N= NY www YA Au خی ی‎ Lu Ch U A JA Ch Ch A 00 oo 一 U UY دیا دیا‎ FA Lë a Un Un Un 一 一 ین‎ hn دی‎ 00 CO 0 OO — Un ما‎ Www — UA Lei Loi iD RB 34 interval 154.1 m 0m 0m base lower 100 m lower 100 m 75.9 m 70 m 86m 103.4 m base lower 100 m 91.2 m 5.9 m 163.4 m base upper mem. ca. 200 m lower 100 m lower 100 m lower 100 m lower 100 m 120 m 120 m 71.1 m 0m 0m 11.4 m 11.4 m lower 100 m lower 100 m 157.4 m 157.4 m 11.4 m 29.4 m 11.4 m lower 100 m upper mem. basal 33.9 m 29.4 m 11.4 m base lower 100 m lower 100 m 140 m upper mem. 1403 m 117 m 34.5 m 5.9 m 137.9 m lower 100 m 29.4 m 102 m basal basal basal lower 100 m lower 100 m lower 100 m formation Blue Fiord Blue Fiord Blue Fiord unnamed unnamed unnamed Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord unnamed unnamed unnamed unnamed Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord unnamed Blue Fiord Disappointment Bay Blue Fiord Blue Fiord Blue Fiord unnamed unnamed unnamed Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Blue Fiord Disappointment Bay Disappointment Bay Disappointment Bay unnamed unnamed unnamed type hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo holo para para para hypo hypo hypo holo para para para holo para hypo hypo hypo hypo holo para para hypo hypo holo para para hypo hypo hypo hypo hypo hypo holo para para hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo hypo species name Stromatoporella perannulata Stictostroma gorriense Stictostroma gorriense Actinostroma sp. A Plectostroma salairicum Plectostroma salairicum Aculatostroma cf. A. kalianum Clathrodictyon ellesmerense Clathrodictyon ellesmerense Clathrodictyon ellesmerense Gerronostroma septentrionalis Gerronostroma septentrionalis Gerronostroma septentrionalis Gerronostroma septentrionalis Petridiostroma sp. Petridiostroma sp. Atelodictyon cf. A. solidum Anostylostroma anfractum Anostylostroma anfractum Anostylostroma anfractum Anostylostroma anfractum Pseudoactinodictyon conglutinatum Pseudoactinodictyon conglutinatum Schistodictyon? sp. Stictostroma gorriense Stictostroma gorriense Stictostroma gorriense Stictostroma? nunavutense Stictostroma? nunavutense Stictostroma? nunavutense Stromatoporella perannulata Stromatoporella perannulata Clathrocoilona vexata Clathrocoilona vexata Clathrocoilona vexata Trupetostroma sp. Trupetostroma sp.? Stromatopora polaris Stromatopora cf. S. hupschii Stromatopora cf. S. hupschii Stromatopora cf. S. hupschii Stromatopora hensoni Stromatopora hensoni Stromatopora hensoni Ferestromatopora cf. F. krupennikovi Glyptostromoides simplex Glyptostromoides simplex Syringostromella zintchenkovi Syringostromella zintchenkovi Salairella prima Salairella prima Salairella prima Salairella prima Atopostroma distans Habrostroma proxilaminatum Habrostroma proxilaminatum Habrostroma proxilaminatum Parallelopora campbelli Parallelopora campbelli Parallelopora campbelli Ottawa. GSC # 108175 108176 108177 108852 108853 108854 108855 108856 108857 108858 108859 108860 108861 108862 108863 108864 108865 108866 108867 108868 108869 108870 108871 108872 108873 108874 108875 108876 108877 108878 108879 108880 108881 108882 108883 108884 108885 108886 108887 108888 108889 108890 108891 108892 108893 108894 108895 108896 108897 108898 108899 108900 108901 108902 108903 108904 108905 110314 110315 110316 BULLETIN 349 Appendix 3.—Collecting locations and stratigraphic position of specimens identified in this study (other than type specimens). Specimens in general collections of the Geological Survey of Canada, Ottawa. Species specimen no. formation interval location Aculatostroma cf. A. kaljanum 110-132 Blue Fiord 76-89 m 1 Clathrodictyon ellesmerense 110-115 Blue Fiord 11.4m 3 Clathrodictyon ellesmerense 110-119 Blue Fiord 67.7 m 2 Clathrodictyon ellesmerense 110-142 Blue Fiord 29.4 m 2 Clathrodictyon ellesmerense 110-263 Blue Fiord 0m 28 Clathrodictyon ellesmerense 110-267 Blue Fiord 0m 28 Clathrodictyon ellesmerense 110-289 Blue Fiord 5.9m 13 Clathrodictyon ellesmerense 110-176 Blue Fiord 35m 6 Clathrodictyon ellesmerense 110-286 Blue Fiord 44.5 m 15 Clathrodictyon ellesmerense 110-135 Blue Fiord 8.9 m 2 Clathrodictyon ellesmerense 110-177 Blue Fiord near base 2 Clathrodictyon ellesmerense 110-248 Blue Fiord 39.6 m 12 Clathrodictyon ellesmerense 110-212 Blue Fiord near base 2 | Clathrodictyon ellesmerense 110-288 Blue Fiord 12m 14 | Clathrodictyon ellesmerense 110-x Blue Fiord near base 1 | Clathrodictyon ellesmerense 111-15 Blue Fiord upper mem. 31 | Clathrodictyon ellesmerense 129-10 Disappointment Bay basal 34 Clathrodictyon ellesmerense 111-24 Bird Fiord near base 20 Clathrodictyon ellesmerense 110-372 unnamed lower 100 m 36 Gerronostroma septentrionalis 110-128 Blue Fiord lower 100 m 9 Gerronostroma septentrionalis 110-172 Blue Fiord near base 4 Gerronostroma septentrionalis 110-179 Blue Fiord near base 4 Gerronostroma septentrionalis 110-189 Blue Fiord near base 4 Gerronostroma septentrionalis 110-191 Blue Fiord near base 4 Gerronostroma septentrionalis 110-238 Blue Fiord 124.3 m 18 Gerronostroma septentrionalis 110-241 Blue Fiord 64.4 m 13 Gerronostroma septentrionalis 110-272 Blue Fiord 44.5 m 15 Gerronostroma septentrionalis 110-327 Blue Fiord 21 m 9 Gerronostroma septentrionalis 110-204 Blue Fiord 17m 6 Gerronostroma septentrionalis 110-309 Blue Fiord 13 m 9 Gerronostroma septentrionalis 110-361 Blue Fiord 13 m 9 | Gerronostroma septentrionalis 110-363 Blue Fiord 77.1 m 10 | Gerronostroma septentrionalis 110-364 Blue Fiord , Vanni 10 | Gerronostroma septentrionalis 110-221 Blue Fiord 124.3 m 18 | Gerronostroma septentrionalis 110-247 Blue Fiord 64.4 m 13 Gerronostroma septentrionalis 110-264 Blue Fiord 39.6 m 12 Gerronostroma septentrionalis 110-156 Blue Fiord 11.4m E, | Gerronostroma septentrionalis 110-342 Blue Fiord lower 100 m 27 Gerronostroma septentrionalis 110-308 Eids uppermost 2p | Petridiostroma sp. 111-1 Blue Fiord base upper mem. 27 | Atelodictyon cf. A. solidum 120-6 Blue Fiord +100 m 22 Pseudoactinodictyon conglutinatum 111-19 Bird Fiord near base 20 Stictostroma gorriense 110-195 Blue Fiord Om 8 Stictostroma gorriense 111-1 Blue Fiord upper mem. 27 | Stictostroma gorriense 111-17 Blue Fiord upper mem. 27 Stictostroma? nunavutense 110-111 Blue Fiord +20 m 2 Stictostroma? nunavutense 110-180 Blue Fiord lower 100 m 4 Stictostroma? nunavutense 110-190 Blue Fiord lower 100 m 4 Stromatoporella perannulata 110-236 Blue Fiord 73.5 m 22 Stromatoporella perannulata 120-3 Blue Fiord 163 m 24 Stromatoporella perannulata 120-7 Blue Fiord 175 m do Clathrocoilona vexata 110-152 Blue Fiord 11.4 m 3 Clathrocoilona vexata 110-182 Blue Fiord 35 m 6 Clathrocoilona vexata 110-322 Blue Fiord 70.3 m Zi Clathrocoilona vexata 110-331 Blue Fiord 70.3 m 27 Clathrocoilona vexata 110-356 Blue Fiord 104.7 m 10 Clathrocoilona vexata 110-362 Blue Fiord 104.7 m 10 Stromatopora polaris 110-117 Blue Fiord +100 m 2 | Stromatopora polaris 110-120 Blue Fiord +100 m 2 Stromatopora polaris 110-129 Blue Fiord 29.4 m 2 DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 41 Appendix 3. — Continued. Species specimen no. formation interval location Stromatopora polaris 110-139 Blue Fiord 154.4 m 2 Stromatopora polaris 110-143 Blue Fiord 210 m 3 Stromatopora polaris 110-153 Blue Fiord 63.2 m 3 Stromatopora polaris 110-160 Blue Fiord 63.2 m 3 Stromatopora polaris 110-184 Blue Fiord 15 m 1 Stromatopora polaris 110-202 Blue Fiord 86.7 m 8 Stromatopora polaris 110-213 Blue Fiord 71.8 m 6 Stromatopora polaris 110-225 Blue Fiord 1403.3 m 5 Stromatopora polaris 110-231 Blue Fiord 1200.3 m 5 Stromatopora polaris 110-233 Blue Fiord 64.4 m 13 Stromatopora polaris 110-251 Blue Fiord 39.6 m 12 Stromatopora polaris 110-252 Blue Fiord 一 21 Stromatopora polaris 110-274 Blue Fiord 1403.3 m 5 Stromatopora polaris 110-286 Blue Fiord 44.5 m 15 Stromatopora polaris 110-299 Blue Fiord 1200.3 m 3 Stromatopora polaris 110-305 Blue Fiord 85.6 m 10 Stromatopora polaris 110-314 Blue Fiord 137.9 m 19 Stromatopora polaris 110-317 Eids 78.8 m below top 17 Stromatopora polaris 110-318 Eids 67.2 m below top 17 Stromatopora polaris 110-320 Blue Fiord 79.1 m 10 Stromatopora polaris 110-324 Blue Fiord 75.9 m 27 Stromatopora polaris 110-333 Blue Fiord 70.3 m 27 Stromatopora polaris 110-338 Eids 65 m below top 17 Stromatopora polaris 110-343 Eids 67.2 m below top 17 Stromatopora polaris 110-347 Blue Fiord 53.8 m 11 Stromatopora polaris 110-354 Blue Fiord 79.1 m 10 Stromatopora polaris 110-367 Eids 85.4 m below top 17 Stromatopora polaris 110-368 Blue Fiord 53.8 m 11 Str omatopora polaris 129-2 Disappointment Bay basal 34 Stromatopora polaris 129-6 Disappointment Bay basal 34 Stromatopora polaris 129-7 Disappointment Bay basal 34 Str omatopora polaris 129-22 Disappointment Bay basal 34 Stromatopora cf. S. hupschii 110-166 Blue Fiord 63.2 m 3 Stromatopora cf. S. hupschii 110-291 Blue Fiord 66.2 m 29 Stromatopora cf. S. hupschii 110-304 Eids 71.7 m below top 17 Glyptostromoides simplex 110-113 Blue Fiord 8.9 m 2 Glyptostromoides simplex 110-201 Blue Fiord 71,1 m 1 Glyptostromoides simplex 110-319 Blue Fiord 146.6 m 10 Glyptostromoides simplex 110-329 Blue Fiord 146.6 m 10 lyptostromoides simplex 110-341 Eids uppermost 23 Glyptostromoides simplex 110-353 Eids uppermost 23 lYptostromoides simplex 110-357 Blue Fiord 146.6 m 10 Glyptostromoides simplex 110-358 Blue Fiord +50 m 9 Glyptostromoides simplex 110-359 Blue Fiord 66.3 m 11 Iyptostromoides simplex 110-371 Blue Fiord 21.0m 3 Salairella prima 110-112 Blue Fiord 46.6 m 2 Salairella prima 110-125 Blue Fiord 11.4m 3 Salairella prima 110-131 Blue Fiord 50.5 m 9 Salairella prima 110-134 Blue Fiord 154.4 m 2 Salairella prima 110-183 Eids 98.4 m below top 4 Salairella prima 110-188 Blue Fiord 154.1 m 1 Salairella prima 110-214 Blue Fiord 71.8 m 6 Salairella prima 110-237 Blue Fiord 86 m 15 Salairella prima 110-250 Blue Fiord 86 m 15 Salairella prima 110-254 Blue Fiord 86m 15 Salairella prima 110-271 Blue Fiord 2100 m 18 Salairella prima 110-301 Blue Fiord 1403.3 m 5 Salairella prima 110-309 Blue Fiord 21m 9 Salairella prima 110-316 Blue Fiord 146.6 m 10 Alairella prima 110-334 Blue Fiord 70.3 m 21 Salairella prima 110-337 Blue Fiord 70.0 m 6 BULLETIN 349 specimen no. Appendix 3.—Continued. Species formation interval location Eids 60.6 m below top 17 Eids +65 m below top 17 Eids 60.6 m below top 17 Eids +65 m below top 17 Blue Fiord +50 m 9 Blue Fiord +100 m 32 Eids 85.4 m below top 17 Disappointment Bay basal 34 Disappointment Bay lower 50 m 33 Blue Fiord basal 2 Blue Fiord basal 16 Bird Fiord basal 20 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 Disappointment Bay basal 34 unnamed lower 100 m 36 unnamed lower 100 m 36 unnamed lower 100 m 36 unnamed lower 100 m 36 Salairella prima 110-339 Salairella prima 110-345 Salairella prima 110-348 Salairella prima 110-349 Salairella prima 110-365 Salairella prima 110-366 Salairella prima 110-367 Salairella prima 129-28 Salairella prima Lowther Atopostroma distans 110-116 Atopostroma distans 110-175 Atopostroma distans 111-25 Habrostroma proxilaminatum 129-3 Habrostroma proxilaminatum 129-4 Habrostroma proxilaminatum 129-5 Habrostroma proxilaminatum 129-8 Habrostroma proxilaminatum 129-12 Habrostroma proxilaminatum 129-14 Habrostroma proxilaminatum 129-15 Habrostroma proxilaminatum 129-17 Habrostroma proxilaminatum 129-19 Habrostroma proxilaminatum 129-23 Habrostroma proxilaminatum 129-24 Habrostroma proxilaminatum 129-27 Habrostroma proxilaminatum 110-215 Habrostroma proxilaminatum 110-226 Parallelopora campbelli 110-244 Parallelopora campbelli 110-278 REFERENCES CITED Döderlein, L. 1892. 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On the stromatoporoids of the Buchan district, Victoria. Royal Society of Victoria Proceedings, vol. 50, pp. 11-45. Rzhonsnitskaya, M. A. 1988. Biostratigraphic scheme of the Devonian of the Russian Platform. in Devonian of the World. Proceedings of the 2nd International Symposium on the Devonian System. N.J. McMillan, et al., eds., vol. III, Canadian Society of Petroleum Geologists Memoir 14, pp. 691-701. St. Jean, J. 1962. Micromorphology of the stromatoporoid genus Stictostro- ma Parks. Journal of Paleontology, vol. 36, pp. 185-200. 1986. Lower Middle Devonian Stromatoporoidea from Empire Beach, southern Ontario, Canada. Journal of Paleontol- ogy, vol. 60, pp. 1029-1055. Smith, G. P 1984. Stratigraphy and paleontology of the Lower Devonian se- quence, southwest Ellesmere Island, Arctic Archipelago- unpublished Ph. D. Thesis, McGill University, Montreal, 328 pp. Smith, G. P., and Stearn, C. W. 1982. 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Stromatoporoids from the Blue Fiord Formation (Lowe Devonian) of Ellesmere Island, Arctic Canada. Journal of Paleontology, vol. 57, pp. 539-559, Franklin). Y.O. Fortier et al., eds., Geological Survey of Canada, Memoir 320, pp. 310-338. Mori, K. 1968. Stromatoporoids from the Silurian of Gotland, Part 1. Stockholm Contributions in Geology, vol. 19, 100 pp. Nestor, H. 1964. Stromatoporoidei ordovika i llandoveri Estonii. Akade- miya Nauk Estonskoi SSR, Institut Geologii, Tallinn, 112 pp. 1966. Stromatoporoidei venloka i ludlova Estonii Academiya Nauk Estonskoi SSR, Institut Geologii, Tallinn, 87 pp. 1976. Rannepaleozoiskie stromatoporoidei basseina reki Moiero (Sever Sibireskoi platformy). Akademiya Nauk Estonskoi SSR, Institut Geologii, Tallinn, 95 pp. Nicholson, H. A. 1873. On some new species of Stromatopora. Annals and Mag- azine of Natural History, Series 4, vol. 12, pp. 89-95. 1886. A monograph of the Britsh stromatoporoids, part 1. 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DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 45 Thorsteinsson, R., and Tozer, E. T. 1962. Banks, Victoria and Stefansson Islands, Arctic Archipel- ago. Geological Survey of Canada Memoir 330, 85 pp. Trettin, H. P. 1978. Devonian stratigraphy: west-central Ellesmere Island, Arctic Archipelago. Geological Survey of Canada Bulletin 302, 119 pp. Uyeno T. T. 1990. Biostratigraphy and conodont faunas of Upper Ordovician through Middle Devonian rocks, eastern Arctic Archi- pelago. Geological Survey of Canada Bulletin 401, 211 pp. Uyeno, T. T., and Klapper, G. 1980. Summary of conodont biostratigraphy of the Blue Fiord and Bird Fiord formations (Lower-Middle Devonian) at the type and adjacent areas, southeastern Ellesmere Island, Canadian Arctic Archipelago. Current Reseach, Part C, Geological Survey of Canada Paper 80-1C, pp. 81-93. Webby, B. D., Stearn, C. W., and Zhen, Y. Y. 1993. Lower Devonian (Pragian-Emsian) stromatoporoids from Victoria. 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Nekotorye devonskie Stromatoporoidea iz okrain Kuz- netskogo basseina, Urala i drugikh mest. Izvestiya vse- soyuznogo geologo-razvedochnyi obedineniva, vol. 50, pp. 1387-1415. 1955. Stromatoporoidea Sovetskogo Soyuza, Part 1. Trudy vse- soyuznogo nauchno-issledovatel’skogo, geologicheskogo instituta, novaya seriya, vol. 8, 173 pp. 1963. Stromatoporoidea Sovetskogo Soyuza, Part 4. Trudy vse- soyuznogo nauchno-issledovatel’skogo geologicheskogo instituta, novaya seriya, vol. 87, 160 pp. Ziegler, W. and Klapper, G. 1985. Stages of the Devonian System. Episodes, vol. 8, pp. 104— 109. Zukalová, V. 1971. Stromatoporoidea from the Middle and Upper Devonian of the Moravian Karst. Ustredniho ústavn Geologichého, Rozpravy, Srazek 37, 143 pp. 1989a. Intraspecific variability and species concepts in Palaeo- zoic stromatoporoids. Association of Australasian Pa- laeontologists, Memoir 8, pp. 45-50. 1989. Specks in the microstructure of Palaeozoic stromato- poroids. Association of Australasian Palaeontologists, Memoir 8, pp. 143-148. 1990. Stromatoporoids from the allochthonous reef facies of the Stuart Bay Formation (Lower Devonian), Bathurst Island, Arctic Canada. Journal of Paleontology, vol. 64, pp. 493- 510. 1991. A revision of Anostylostroma, Atelodictyon, and related genera (Paleozoic Stromatoporoidea). Journal of Paleon- tology, vol. 65, pp. 611-622. 1992, Petridiostroma, a new name for Petrostroma Stearn, 1991, not Petrostroma Dòderlein, 1892. Journal of Paleontology, vol. 66, p. 531. 1993. Revision of the order Stromatoporida. Palaeontology, vol. 36, pp. 201-229, 19954. The type species of Stictostroma Parks, 1936 (Porifera, Stromatoporoidea). Journal of Paleontology, vol. 69, pp. 20-27. 19950. Stictostroma Parks, 1936 (Porifera Stromatoporoidea): proposed conservation and designation of S. gorriense Stearn, 1995 as the type species. Bulletin of Zoological Nomenclature, vol. 52, pp. 18-20. Stearn, C. W., and Mehrotra, P. N. 1970. Lower and Middle Devonian stromatoporoids from northwestern Canada. Geological Survey of Canada Paper 70-13, 43 pp. Stearn, C. W., and Pickett, J. 1994. The stromatoporoid animal revisited: building the skel- eton. Lethaia, vol. 27, pp. 1-10. Stock, C, W. 1979, Upper Silurian (Pridoli) Stromatoporoidea of New York. Bulletins of American Paleontology, vol. 76, pp. 289-389. 1982, Upper Devonian (Frasnian) Stromatoporoidea from north- central Iowa: Mason City Member of the Shell Rock For- mation. Journal of Paleontology, vol. 56, pp. 654-679. 1984. Upper Devonian (Frasnian) Stromatoporoidea of north- central Iowa: redescription of the type specimens of Hall and Whitfield (1873). Journal of Paleontology, vol. 58, pp. 773-788. 1989, Microreticulate microstructure in the Stromatoporoidea. Association of Australasian Palaeontologists Memoir 8, pp. 149-155. 1990, Biogeography of Devonian stromatoporoids. in Palaeo- zoic Palaeogeography and Biogeography. W.S.McKerrow and C.R.Scotese, eds., The Geological Society Memoir 12, pp. 257-266. Thorsteinsson, R. 1980. Stratigraphy and conodonts of Upper Silurian and Lower Devonian rocks in the environs of the Boothia uplift, Ca- nadian Arctic Archipelago, Part 1, Contributions to Stra- tigraphy. Geological Survey of Canada Bulletin 292, 38 pp. 1986, Geology of Cornwallis Island and neighbouring smaller islands, District of Franklin, Northwest Territories. Geo- logical Survey of Canada, Map 1626A, Scale 1:250,000. BULLETIN 349 EXPLANATION OF PLATE | Figure ACOSO dd y YA HI pd DT T 14 Specimen GSC 108852. 1. Vertical section, X 10. 2. Vertical section, detail of pillars diverging from low mamelon; x 10. 3. Tangential section; x 10. ee EE r ß CON TEL TE 15 Specimen GSC 108853. 4. Vertical section; x 10. 5. Tangential section; x 10. 4-5. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE | P LEE ۳ "iM CN Cf ۱ a KL De a NR ; WAA A figit Zi ie 1 M e data QUE EM e ket = US $ r era 19 RISA a OE e eR و‎ d Sieg gie Si Mns x M DE: e A Sl AM "iu oi TË a e dE wm ¿O و‎ ee Na LI A e Lowe Ve ih ۱ dt hm 3 MRS See. se و‎ e EE pec cda BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 2 LÀ hi ا‎ > T Co E) DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 47 EXPLANATION OF PLATE 2 Figure Page -5 Aculatostroma cf. A. Kalanumi(Bogovavisnskaáva, M rana 16 Specimen GSC 108855. 1. Vertical section; x 10. 2. Tangential section; x 10. 3. Hand-specimen, slabbed surface; X2. Note pattern and distribution of astrorhizae. 4, 5. Vertical section, detail of colliculate pillars. Same view at x 100 (Fig. 4) and x 250 (Fig. 5). BULLETIN 349 EXPLANATION OF PLATE 3 Figure Page 13. Clathrodictyon ellesmerense Steam, 1983. |... Wine Coreen ß 0498 ٩ 17 1. Vertical section; x 10. Specimen GSC 108857. Note successive phases of growth (rhythmic variation of laminar spacing). 2. Vertical section; x 10. Specimen GSC 108856. 3. Vertical section; x6. Specimen GSC 108858. Note the impersistent protuberances, unlike mamelons. 4-5. Gerronostroma septentrionalis, new species; dea he eet had dere i 18 Paratype GSC 108860. 4. Vertical section; x 10. 5. Tangential section; x 10. E 109 ۱ td : £ 1 ۳۹ a) —.— gi 4 LI as » 4 A A 3 = Rit ۹ e 3 - TD Jet dm) by tak > E KN Lue o T "wh 7 + poe x وم‎ : Reg R n 4 : : Theta ion Eren " er re ny ۲ » Area > dh lidd, A gens 1 ** LII spe 3 n PA tek f t ee ee EAP ai to " 7 dE 7 5 24i e SITA JI A er sia ال‎ st 3 si, n NEE, د‎ T ein oj .h ; . eeng pe LIO ha diaris E ANS v n] و‎ „10+ تع ارت و ر‎ ares ا‎ Lei LAT a e ربياه كم‎ e و‎ : 4 Prvou Ne PN ir wen, SCH KEN LEE hs 9 n E [^ < Ne a "linn e E LL Ce TT A Mata Läit: ass: AUD ry Nb A * E دي‎ e AP PITTI < e DNA Para ei Bene ۹ e E? fle. d € r è 3 2 Aë og. SI de Aul Ge 28 DEER 8 eng der ع‎ ma WE SPA و‎ arp AE 88 و‎ ee NA... Te deva Witton. ri or E ? RATTO * [NN NC وه ورج‎ — me 9988 A vo e Er P | wid. ووو‎ TIR V x» PASO. wapa arde Vet Age y came piva Ers "i ۷ 11039 0 جح‎ عمجيو وه ووه‎ AP rem, + * 0 M aA e A ARD e, Aotre d n II ds Ata Fe) P m8 as Kk Dic m LJ Og MMMRRUM soten, à Matgen, ase rie i -— ۱ ۰ kaa موسا‎ " Ge 2 E v reir. Panino — ri ^ De CADA جو وميد ووو موه‎ a V DANÁ ow: 0 Lievens d AE POM bý شد‎ e + " ius UM SM n dea dris vem en HEN * Se ep der, "ft n M ee * f MT eit O ee Sane ii SA ^" NX 770 ve BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 9 HX) Tan Magy e... 4 Co EN, sh 4 de. Ple ne, Ka عع‎ Bel a cames ° — DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 49 EXPLANATION OF PLATE 4 Page La, EE SEDIENITIONGUIS, ME yd sS 18 1, 2. Holotype GSC 108859. Vertical section (Fig. 1) and tangential section (Fig. 2); x 10. 3. Paratype GSC 108862. Vertical section; x 10. Note abundant commensal syringoporids. 4. Competitive overgrowth relationship between holotype G. septentrionalis n. sp. (left, upper) and Stromatopora polaris (right, lower). GSC 108859. Vertical section; x 5. BULLETIN 349 EXPLANATION OF PLATE 5 Figure Page 19 1 POT OMICS eee ON Specimen GSC 108863. 1. Vertical section; x 10. 2. Tangential section; x 10. 3, 4, Atelodictyon cf. A. solidum Khromych, 1976.lSmf ] œ ́U:1) ! 5? یی‎ 20 Specimen GSC 108865. Note: thin-sections photographed under reflected light. 3. Vertical section; x10. 4. Tangential section; x10. Lë we $ ET? re ack Ts o ا‎ RASO BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 6 24 i Jee Bee 14 vo La ta f DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 51 EXPLANATION OF PLATE 6 Figure 1-5. Anostylostroma anfractum, new species. 1. Holotype GSC 108866. Vertical section: x 10. 2. Holotype GSC 108866. Tangential section; ۰ 3. Paratype GSC 108867. Vertical section: X 10. . Paratype GSC 108869. Vertical section; x 10. . Paratype GSC 108868. Tangential section; x 10. ns 52 BULLETIN 349 EKPLANATION OF PLATE 7 Figure Page RARO I ARA O EEA E TA AE 22 1. Holotype GSC 108870. Vertical section; x 10. 2. Holotype GSC 108870. Tangential section; x 10. 3. Paratype GSC 108871. Vertical section; x 10. 4. Paratype GSC 108871. Tangential section, x 10. j 2 二 Specimen GSC 108872. 5. Vertical section; X 10. 6. Tangential section, X 10. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 8 tý x. e رن‎ ES hat V * Ze Praes d A SE ee . 53 DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN EXPLANATION OF PLATE 8 o, Stictostroma SO ONE enn , ñxõß a a yS . Vertical section; x 10. Specimen GSC 108177. Vertical section; x 10. Specimen GSC 108874 . Tangential section; x 10. Specimen GSC 108177. . Vertical section, detail of microstructure; X 50. Specimen GSC 108874. . Tangential section, detail of microstructure; X 50. Specimen GSC 108875. Figure 1 — — ھچ مها | BULLETIN 9 EXPLANATION OF PLATE 9 Figure Page 25 和 1. Holotype GSC 108876. Vertical section; ۰ 2. Paratype GSC 108877. Vertical section; x 10. | 3. Holotype GSC 108876. Tangential section; ۰ 4. Vertical section, detail of microstructure; X 25. Paratype GSC 108877. 5. Tangential section, detail of microstructure; x25. Paratype GSC 108877. B 50 N C IGY 0 " 2 s 0 ET A eun * » A BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 b Be, we HA Y در‎ Sian, P yot a 08 ل‎ ۶ um ¥ a uy " m te Toad eon 4 A DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 55 EXPLANATION OF PLATE 10 Figure Page 1,2, Siromatoporella perannulara Galloway and St. Jean, lo,, 8 26 Specimen GSC 108175. 1. Vertical section; x 10. 2. Tangential section; x 10. 28 Clathrocoilona vexata, new Pe) VV A SN Holotype GSC 108881. 3. Vertical section; x 10. 4. Tangential section; x 10. 3, 4, BULLETIN 9 EXPLANATION OF PLATE 11 Figure enn d RARA ß ANS Detail of microstructures; all figures x 50. . Tubulate microstructure; tangential section. Holotype GSC 108881. . Tubulate microstructure; vertical section. Paratype GSC 108883. . Tubulate microstructure; vertical section. Holotype GSC 108881. . Vermiculated or felted microstructure; vertical section. Paratype GSC 108883. . Compact microstructure; vertical section. Paratype GSC 108883. . Blocky or melanospheric microstructure; vertical section. Paratype GSC 108882. . Melanospheric microstructure; tangential section. Paratype GSC 108882. . Ordinicellular microstructure (centre of field); vertical section. Holotype GSC 108881. co NO U ll YN PLATE 11 BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 12 E s‏ لعو A‏ DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 57 EXPLANATION OF PLATE 12 Figure Page 1,2, Clathrocoilona vexata, new Seel), 28 1. Paratype GSC 108883. Vertical section; x 10. 2. Paratype GSC 108882. Tangential section; x 10. 30 3, 4, CCTV) yd DN U. Specimen GSC 108884. 3. Vertical section; x 10. 4. Tangential section; x 10. 58 BULLETIN 349 EXPLANATION OF PLATE 13 Figure Ll SPO ONO ” fr dd ß 31 1. Vertical section; x 10. Specimen GSC 108887. 2. Tangential section; x 10. Specimen GSC 108889. % P EE ̃ͥ ͤů o الو و كلوه‎ CG EN reso EE EE 32 3. Holotype GSC 108890. Vertical section; x 10. 4. Holotype GSC 108890. Tangential section; ۰ 5. Paratype GSC 108892. Tangential section; x 10. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 13 PLATE 14 AA ۷ È ۳۹ E CX? im fi Kier Le: AP Ae 3 24 at 38 M Si GE e ۷ 9 rg È 5 a M Ce Le Tw dE ^ s. DË RE i ae ^ M 4 ria N 1 get a asi me: ba oy 4 2255 aW? eech BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 9 v» "i 9 A iu Ce e DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 59 EXPLANATION OF PLATE 14 TR Page 1,2, | erer ch P. krupennileont Yara, 1988. . N Specimen GSC 108893. I. Tangential section; x 10. 2. Vertical section; x 10. 3 ae Glyptostromoides simplex LECH, جم م‎ ß م‎ m 33 3. Tangential section, X 10. Specimen GSC 108895. 4. Vertical section; x 10. Specimen GSC 108894. 31 + Stromatopora LEE wa LOSE PR RE ARTI ee a NE Vertical section; x 10. Specimen GSC 108886. BULLETIN 349 EXPLANATION OF PLATE 15 60 Figure 1-3. Syringostromella zintchenkovi halina, 1961). 40. ey f 8 34 1. Vertical section; x 10. Specimen GSC 108896. 2. Tangential section; x 10. Specimen GSC 108897. 3. Tangential section, detail of microstructure; X 25. Specimen GSC 108897. Fan aao! Sor Oa TT 34 4. Vertical section; x 10. Specimen GSC 108898. 5. Vertical section; x 10. Specimen GSC 108899. 4, 5. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 15 RA ; MILA Mii CA) "Was À اليس‎ a A VW ^ Fm LAN, Kg Mete > ٠ * 3T. 5. 3 ak: نا‎ | mu BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 16 DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 61 EXPLANATION OF PLATE 16 Figure Page 75. Salairella prima 961356157 IITE a A INU 34 1. Vertical section; x 10. Specimen GSC 108900. - Tangential section, x 10. Specimen GSC 108899. . Tangential section; x 25. Specimen GSC 108899. Note the smooth termination of cellules bordering skeletal galleries. - Tangential section; x 25. Specimen GSC 108901. Note the ragged termination of cellules bordering skeletal galleries. . Vertical section; x 25. Specimen GSC 108898. Note the local development of microreticulate microstructure. 1 U 4 0 iD | 62 BULLETIN 349 | EXPLANATION OF PLATE 17 Figure Page F %%% IRA EE 36 1. Vertical section; x 10. Specimen GSC 108903. . Tangential section; x 10. Specimen GSC 108904. . Vertical section, detail of astrorhiza; x 10. Specimen GSC 108905. . Vertical section, detail of microstructure; x 25. Specimen GSC 108903. . Tangential section, detail of microstructure; x 25. Specimen GSC 108903. AUN BULLETINS OF AMERICAN PALEON LOGY, VOLUME 109 PLATE 17 wu MM: ORE mi N "i * M eat z‏ رک ži E La‏ ی Së‏ AF BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 109 PLATE 18 ^ IA ١ P 4% 1 A ag 17 wes Sa E las 224% » ` CA + bi. pe È 4 ۰ e A», 22 at 21 IA “e a ata LA pe $ Sa he EE DL Bé KT: DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 63 EXPLANATION OF PLATE 18 | Figure laa, Parallelopora E ni AA ͥJ2 a EEN 37 I. Vertical section; x 10. Specimen GSC 110314. 2. Tangential section; X 10. Specimen GSC 110316. 3. Vertical section, detail of microstructure; x 25. Specimen GSC 110314. 4. Tangential section; detail of microstructure; x 25. Specimen GSC 110316. Atopostroma distans (Ripper, A ی‎ AA 36 Vertical section; x 10. Specimen GSC 108902. Di | BULLETIN 349 INDEX Note: Page numbers in italics indicate the location of the taxonomic description. Plates are indicated by the page numbers of their captions in boldface. Authors are indexed only where their name appears in the text discussion, not in references. The abstract and bibliography are not indexed. Names appearing on text figures are indexed by page and figure number (eg. 7-۳1 = page 7, figure 1). e eee, ,,,, 31 e . SI NT 29-30 hn E 11 ká ,,,, EE 27-0 ůÜ h 27, 28 dd T T US 28 ارو دی‎ soie omm OUT EE 15 ۵ Ie CUN A Re RR NIU AED Ian s 29 dd bo RC E 29 PO M TU m 29 RIE EC AUC Ie e T m 30 OBIIT E CR RC C TOTO ebur EIN 29 f,, 29 ONDA ite cs EE 29 SD NE A ec 29 ,, ß 30 r 5, 12-F3, 28-30, 39, 40, 55, 56, 57 SIEM ال‎ KANA !!!! RAO rei 17-26 brannte ا‎ ere EU ees 17-21 MA a 17-18 ,,,, De خر‎ 26 MIDA atk ممم لمعم‎ 5, 12-F3, 17-18,39, 40, 48 VICI 17 Cielo O a. 11 14 ,,,, ñßßß ere GP cient AA 31 GONE US t 27, 38 Somme 17, 9 27 POMOTE A erian e te CÎ 13 % 9-11 (yla A EE 8-F2, 9-11, 12-F3 Fl dvn 6, 10, 11 GO MWANI SANI rami ayes nee RN 6, 7-۳1, 9, 10 GE d ern I E F2, 9-10, 11 e eee, EE 15, Detroit River Group ................... 11,23, 27, 35, 0.8 DECORADO irs) Soe o LOS ORE OE aet 7-F1, 8,2 IDIABSITOSIE o Rm do 4 Lie COL e DUCERE 17 erte eln. 14 “/ روه ران بلعو‎ O AAA 23 Disappointment Bay Formation ................. 6, 8-F2, 8, 9, VV 10, 18, 31, 34, 35, 37, 39, 41, 42 Dundes POMENOM mn Vii EYE 3 .. . o 9, 16, 32, 37, 38 erf ,,, EE ra و‎ 11 CC 5, 7-۳1: 17, 27, 31, 32, 33, Fids Formation ......... 6, 9, 10, 19, > 32, 33, 35, 40, 41, 4 Ellesmere Island .................... 5, 6, 7-F1, 8, 10, 17, 1 ER IS 20, 23, 25, 27, 30, 31, 39 Reet aa 9, 10, Il RARO i 28. 37 a NM m EE EE eee, IQQ DUIS 32-33 %%% A 12-F3, 33, 39, > AA V او‎ ció % ͤͤ wuBöe.... 14, 15, 16 JCPUf ].... 88 14, 15 777... 8 15 DET SIRES TEA ES 15, 39, 46 SAI 15, 16 i E 12-۳3, 14, 15, 39, 46 %%% E II 36 f ES ere eg te, 15 %%% ² ² ñNkꝛw æ pxp m BATI 14-7 VVV%V%V%%%S// ( ae وا و‎ tes 14-17 J)) os wees لع‎ NP Tn 16-17 %%% Ä 8 11, 12-۳3, 16-17, 19, 39, 40, 47 BODIE CECT TE رار اجا رار واج‎ POET وو‎ 16 akosmoreticulate microstructure veis ie erem ia 29, 30 a i 6‏ لل IO lr 9 ARO OT OIN و ور‎ (edo v ER ABER AAA 21, 24 lf v 12-۳3, 21-22, 39, 51 % age e ول د هم‎ 20 VOU CI ie Me des BT TE E 9/۳ a EEN 21 OS a E S T 19, 20 Aree AnD EE eere ea re Ora en AAA 5 NRE 11 7 8 , ا امس م HCH‏ ren ی موی‎ de e rey طعي‎ 8 14 e HEC c ne OE 17, 20-21 ebd SOUGHT er ena venir ve 11, 12-F3, 20-21, 39, 40, 50 EA A ie cer UP ne oa 11, 20-21 SE EE on AA rene CE UTE LT 20 roa 19, 35-6 INCAS OU E E I 5, 11, 12-F3, 36, 42, 63 OI v5 20 2 e lil ae 8 11, 24, 34, 35, 36 DIO 5r md C 17, 13,19) —.. ͤ .:.. ere عمجم‎ zá 6, Fl, 9, LU, LI, T5, ** 16, 17, 18, 19, 20, 22, 8 Bent Porn ع‎ dire i rea TV معنم‎ Gans VETA YA 6 Lali ) «²”d. yx 7 Biostratigraphy, stromatoporoid ....................... 11-13 CJ%00%%% ir La هه مر‎ RS 9 BO ... هو مح‎ er rent AA AAA 9,6 Bird Fiord Formation ........ 6, 8-F2, 9, 10, 17, 18, 23, 40, 42 bruce rs rere ro ns Es 30 bee ria 38 %%% li و دو‎ ener ا‎ rar V VV 6, 7-F1, 10 Blue Fiord Formation ........... 6, 8-12, 8, 10, 17, 18, 19, 20, 52122 24, 25, 20, 27, 30,31, 32, 33, 3A, 35; 2 C —(—-„—ñ ner creer nana ĩͤ ER 17,18 J%%%%%C%%́! ß piss, a) y الود ع مر‎ ČO عمو وام‎ EE 0, 10 Buchans Cave Limestone, Australia ............ nn 36 PUSY IC LET RIBA DOLIZON A RE 31 %%% AAA , ĩ NEEN ER 17 i sb O 38 DEVONIAN CANADIAN STROMATOPOROIDS: PROSH AND STEARN 65 ,.. TT 35 MIMO TEA E, | 28-30 MIOT OIA eee 8 26 ht ee cate EE 83 Jed e eff) Do DOROIN AO vi e 8 14 Microlubulate:mucrosiriciute i Gn 26 Mondrian 23 MONOLOGON Vara EE 13 MEKON eff 6, 7-F1, 8-۳2, 8, 10, 21, 27 Masi fs 8 19 Natural Sciences and Engineering Research Council ......... 6 an,, EO eU oc TEE ci 21 39 Norwegian: Bay Meme 8 9 %%% m dd ANO UTE 23 eff 8 23, 21, 30 | ji Omulevski MOUNIBINS; SIDONIA cielo ra rie ds 21. 39 hre ee rere a EL 27 ee ei 1]. 23. 4 Fr ß يي‎ ri CC a 11-13, 38 EE EE IO CS ela 11, 12-F3, 37-38, 39, 42, 63 FOPHUSIDSITOME ev a ye حا كا لس‎ 31 aten 8 17 „ ² « OR ES re ee 10, 15 Sn EE 10-11, 15 Pentamerus pseudobaschkiricus beds vc 15 %%% ce cls eR A RE 19-20, 23, 4 ll ia ال‎ EE 12-۳3, 19-20, 39, 40, 50 PROSA sen eis mr; EE 19 Phases LL LIRE Re ey ee EE 17, 16,19 SUI 0 ا‎ E 18 Ii يال ل ا ابا‎ EE 23 Platform, North American poesies RE لحك‎ a عون ادي‎ 5 %%% ²ᷣͤ v.. ð RO A I ممع‎ ae 19,16 EEN ff ov AAA 16 ff ð y t مج ا‎ 16 . a TT 16 Ml 11, 12-۳3, 15—16,39, 46 Polar CONTINENTAL eee 6 PONENAMUSAH P. DETOONUS iii 9 BOINA MUS REIS d 10 PONENAMUS SPONDING na 9 d A¶ͥͥ 8 9 V ²⁰ ß US gui te hd w EE 10 Port Colborne, Niagara ars n nn 27 Preservation, /nſnön„nn 8 17 // ᷣ 13-4 eee 22-23 PJ 22 m,, تود‎ be 11, 12-F3, 22-23, 39, 40, 2 Reef TRUDE es tiv Cen ect a eae RA IE CCCII Eo et eres 5 d,, ⁊ ⁊ EE S | 9 RESQUE NR aaa 7-۳1 hne. 8 14 Russia, see specific districts T7 ͤ ll 327 33 Molla , E ds 31 N or ͤ 15 Formosa ies Pa ia eege 275-9. ©. Fs LUE DL WAA E 28, 29, 38 Geological r ا‎ ea 14 Gerr, ANA A اع‎ raaa ا‎ occ اللا‎ A 18-9 me moran ee 5311139 elegans a a Cer T am CRGO RS A MEER 18 LIE YE A 19 eee, 5, 12-۳3, 18-19, 26, 39, 40, 48, 49 Sp. A EE EE EE 18, 19 AMAT oi wee co ل‎ ree 19 Glyptostromoides REE eee n ca 33 E ve CC 5, 12-۳3, 13, 33, 39, 41, 59 BEEN Serene ee 10 E UT ee 6, 7-F1, 8-F2, 8, 10, 20, 27 7; N S 8-F2, 9-10 Bau competitive As E ااا‎ ORUM 19 ea 18 Habrostroma e ا‎ E 36-7 densilaminatum A RACE A AAA 36 Tute ل‎ ee Ce 36 Proxilaminatum `... 11, 12-F3, 36-37, 39, 40, 62 %%% ا‎ 30-31 ee 11 | are ع‎ ES 22, 38 EE Tersonville eee E 2738 ne, Australia... "akuter ug a 11, 35, 6 Kara-Chumysh IC no 15 tie ͤ 16 A a A LA 5 BREED ic 38 JJV 10 EM ost ˙•0 ل‎ e 34 الل اا‎ ⁰²ð¹ꝛmĩ ˙⁰¹ꝛ im ca aa * 16, 21, 34 ال‎ anaes 9 yy) a Skovski UA BE Ee GE E 34 echte d. 5 ati قد د‎ H GIRCUSSION: 23 ` anioni 17 4 28 ry وو‎ E Ee Rives, Australia: wina PS 34 Toy. etre o 6 ther Island 6, 7-F1, 9, 10, 35, 8 u a „ ee ee ee NI LOLA ER D m H H > 3 8 Formation Vara SR با‎ I IRON ee EE 38 Malo ame, chatski ROM AON stresové a يون‎ T 34 in Saran رت‎ ecd 30 M lehead, Ohio 2 4 EN U : i e E 8 icr, ents, ness to yee er ets 14 S tructure, discussion SMoreticulate eu 29, 0 STO 2 ^ | | | BULLETIN 349 a s 5-9 IT 19, 20, 36 See 13 synonymies, general comments 13 Syringodictyon tuberulatum i. الل حيو و ري‎ 8 5 7. tae, DEE 17, 131 sgr EE 35-37 SYTINSOStO MARS ce e 35-37 % VENPUGOSUMU li A 16 V TOR 33-34 . ( 34 REI sn i a 11, 12-۳3, 34, 39, 0 AA RO ا‎ AR A A 34 a Mabie cn) ty سنن‎ aa 33-35 Systematic DEET رع و‎ oe cere 13-38 WEEN , I 21 Terminology, ee eee, 14 TINI doc لوو وده روود رفم‎ ia ra E 21 Tippecanoe SEQUENCE. iii EE VN 5 ET ue ل ع‎ RI E 6, 10 EE, 30-31 CIONI ina 30 (Elo) (APRITE A ENEE 36 C6IgI d SEA RI 31 BORN 31 a وقلع را‎ ey ممع‎ A E E 30 ea a I 11, 12-F3, 30, 39, 57 / radi VA RR 30 % f,, VA OT COLI Gd TN LIA 30 Truro Island ......... 6, 7-۳1, 9, 10, 15, 18, 31, 32, 35, 37, 88 Type specimens, repositoty e eren è ñ 0]᷑ 14 EIDEN, 21 United States, north-central EN Mion 11 CCC 6, 8-F2, 9, 10, 11, 15 aereo 18, 32, 37, 38, 39, 40, 42 Urale ما‎ Russi: rr 1116 DS AE ci teo E 9,1 ILL و‎ 19, 23, 31 Väriability, morphologie ses re TV 13 RIT ل ل‎ oN oe 6, 7-F1, 9, 10, 17, 1% iu 19, 20, 25, 27, 30, 31, 32, 35, 36 Nato tis: e f I 11 JJV 11, 13, 24, 35 ee e وتو‎ Ca WAA 15, 33 Zdimir pseudobaschkiricus beds rse rier: vice . 15 , ree ی‎ 19 A IA A r id 11, 24, 5 نب‎ A A enema te WW EE 53:28, 29409 Sl NASL) هم‎ ani «us حل‎ 11, 34 %% وم‎ sr ار‎ SR ا‎ 34 ea 34 e, SE 5, 11, 12-۳3, 34-35, 39, 41, 42, 60-61 da Enn n ˙ - A EE 22 . EE 20, 23-24 ADA EE en n cus ع‎ dE DES 24 ej RE 20 %%% 88 12-F3, 23-24, 39, 52 BODIES crei e a iii SAI 11 . is EE 10, 11 ,,,, دورو‎ Emrê ome tora 11-35 ee e NE oo ب لد بع ی را + الى‎ ee DENT 11.285 ttt amenacen en as 7%) O ya r Da rg او ا‎ 49 UNO اسار عه جعي ( و‎ ent oie do SO 19 CELA us ß „ CCTV 3, 6, , SA, 700000 dT nie rr 15 B ره‎ ß رم‎ k 24-26 ))) ont ties atra e a es 29 و وم ᷣ د ووه‎ Tere 8 13 EIERE E 26 IIA AA T 11, 12-F3, 24-25, 26, 39, 40, 53 SUI a عع ةنوم‎ AREAS AAA 24, 25 Lal 11,24: 25 77 RR ور‎ A b né ee E 24, 25 EE AA 25 Stictostroma? nunavutense ........ 12-F3, 19, 25-26, 39, 40, 54 UAA]! ²⁵²[nii. md EOI CI 24-30 OL بيع عي ی‎ O ع لم‎ rt errr do 6, 16, 28, 29 ,,, een pere nn 12-F3 % ² ²õ — vi COREE IA pe 31-2 COS و‎ ess Part 5, 12-F3, 31-32, 34, 39, 41, 58 BIB EE 21 O و‎ AR يج‎ UA ی وه‎ Er, 34 OD و‎ ⁵ d ¼ d ĩ ĩ ĩ VA SA VN A ار‎ %%% ET A 13 VAŠO as osv ARE وج ووه‎ 12-F3, 31, 32; 99, 58 iii 8 32 pst fas ددعم رع الا‎ ⁵mm ور‎ EE 24 1012] 21 RATO 5, 11, 12-۳3, 19, 31, 32, 39, 40, 41, 59 %.... y ⁊ O RUP UE 36 JJ) ꝙ ↄ erin bane y ts leg ei ECT 34 DINO Fre رع‎ at وو‎ ete ĩ الوا‎ YS 26-27, 29 CAMINO, sate eS وعم م برع‎ O A 00 26 COU -m ĩðͤ d ⁰ꝛx ا‎ 15 VV 26, 27, type specimen 27 DET ع‎ na tá dza فط‎ 11, 12-۳3, 26-27, 39, 40, 5 Stromatoporellida: مریم‎ «eo Qeli 8 24-1 e, d 31-5 eo ido ار ع‎ roa ry ens 31-3 PREPARATION OF MANUSCRIPTS Bulletins of American Paleontology usually comprises two or more sep- arate papers in two volumes each year. 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