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Cretaceous Research 30 (2009) 939–951

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Cretaceous Research

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Molluscan biostratigraphy and paleomagnetism of Campanian strata, Queen Charlotte Islands, British Columbia: implications for Pacific coast North America biochronology

James W. Haggart a,*, Peter D. Ward b, Timothy D. Raub c, Elizabeth S. Carter d,1, Joseph L. Kirschvink c a Geological Survey of Canada, 625 Robson Street, Vancouver, British Columbia V6B 5J3, Canada b Department of Geological Sciences, University of Washington, Seattle, WA 98195-1310, USA c Division of Geological and Planetary Science, California Institute of Technology 170-25, Pasadena, CA 91125, USA d Department of Geology, Portland State University, Portland, OR 97207-0751, USA article info abstract

Article history: A previously uncollected fauna of ammonites, bivalves, and other molluscs, associated with radiolarian Received 9 June 2008 microfossils, has been newly recognized near Lawn Hill on the east coast of central Queen Charlotte Accepted in revised form 13 February 2009 Islands, British Columbia. The regional biostratigraphic zonation indicates that the Lawn Hill fauna is Available online 3 March 2009 correlative with the Nostoceras hornbyense zonule of the Pachydiscus suciaensis ammonite biozone, recognized in the Nanaimo Group of southeast Vancouver Island. The Nostoceras hornbyense Zone (new) Keywords: is herein proposed for strata of Pacific coast Canada containing the zonal index. Several molluscan taxa Campanian present in the Lawn Hill section are new to British Columbia and the ammonite fauna suggests that the Maastrichtian Ammonite Nostoceras hornbyense Zone is late Campanian in age, supported by radiolarian taxa present in the Inoceramid section. Strata sampled in the Lawn Hill section preserve reversed-polarity magnetization, considered Magnetostratigraphy likely correlative with Chron 32r. The presence of the Nostoceras hornbyense Zone on Queen Charlotte Queen Charlotte Islands Islands is the first recognition of this zone in Canada north of central Vancouver Island and represents the youngest Cretaceous known in this region. Campanian radiolarians identified from the Lawn Hill section are also the first recognized from the Pacific coast of Canada. Crown Copyright Ó 2009 Published by Elsevier Ltd. All rights reserved.

1. Introduction several morphogeological provinces of the Canadian Cordilleran region and includes the offshore island systems of western British Cretaceous strata are distributed widely across Queen Charlotte Columbia and Alaska, including the island systems of Queen Islands, British Columbia (Haggart, 1991, 2004), with major outcrop Charlotte Islands and Vancouver Island in British Columbia, and belts found in the Langara Island to White Point region on the parts of the southeastern Alaska archipelago (Fig. 1). northwest coast, and in the Skidegate Inlet and Cumshewa Inlet The principal geological components of the Insular belt are the areas of the central part of the islands (Fig. 1). Cretaceous strata are Wrangellia and Alexander terranes, the former well developed on inferred to be distributed also in the offshore regions adjacent to Queen Charlotte Islands, the latter in southeast Alaska. The Baja Queen Charlotte Islands and collectively, these deposits accumu- British Columbia (‘‘Baja BC’’) hypothesis proposes large-magnitude lated in the Hecate basin (Hunt, 1958; Haggart, 1993; Mossop et al., northward translation of, at minimum, the Wrangellia terrane of 2004), inferred to have developed in a fore-arc setting westward of the Insular belt relative to the North American craton during Late an active magmatic arc (Haggart, 1991, 1993; Higgs, 1991; Thomp- Cretaceous and Early Tertiary time. The hypothesis remains son et al., 1991; Lewis et al., 1991; Lyatsky and Haggart, 1993). controversial (Mahoney et al., 2000; Enkin, 2006) as the paleo- The Hecate basin accumulated on a varied topography of older magnetic data upon which it is based (i.e., Bogue et al., 1995; Ague Mesozoic and Paleozoic(?) sedimentary, volcanic, and plutonic and Brandon,1996; Irving et al.,1996; Ward et al.,1997; Housen and rocks collectively assigned to the Insular belt. This feature is one of Beck, 1999; Enkin et al., 2001, 2003; Haskin et al., 2003; Housen et al., 2003; Bogue and Gromme, 2004; but see Stamatakos et al., 2001 and others) are methodologically sound yet seemingly con- tradicted by numerous geological and paleobiogeographical infer- * Corresponding author. E-mail address: [email protected] (J.W. Haggart). ences (i.e., Mahoney et al., 1999; Butler et al., 2001a,b, 2006; 1 Mailing address: 69745 Old Wagon Road, Sisters Oregon 97759, USA. Kodama and Ward, 2001; but see Miller et al., 2006).

0195-6671/$ – see front matter Crown Copyright Ó 2009 Published by Elsevier Ltd. All rights reserved. doi:10.1016/j.cretres.2009.02.005 940 J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951

Fig. 1. Location map of Queen Charlotte Islands, British Columbia, showing location of Cretaceous (Campanian) outlier at Lawn Hill. Area of Cretaceous Hecate basin indicated in grey in inset. AT ¼ Alexander terrane, WT ¼ Wrangellia terrane. Note inferred paleo-high separating Cretaceous Hecate and Nanaimo basins of west coast Canada.

We present herein new paleontological and paleomagnetic data Columbia, some 650 km south of Queen Charlotte Islands. In from Upper Cretaceous (Campanian to lowermost Maastrichtian?) addition, while the paleomagnetic data are considered of insuffi- strata of Queen Charlotte Islands. The faunal data establish for the cient quality and number to establish a paleolatitude suitable for first time the presence of upper Campanian strata on Queen paleogeographic analysis, recovery of reversed-polarity magneti- Charlotte Islands, with correlatives exposed in southern Alaska and zation in calcareous concretions sampled in the section is consid- on Vancouver Island and associated islands of southwestern British ered most likely correlative with Chron 32r (ca. 71–73 Ma). J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951 941

2. Regional geological setting accumulation in a stable tectonic setting (Haggart, 1991, 1993; Lewis et al., 1991). Continuous deposition initiated in Valanginian time and Wrangellia terrane hosts sedimentary basins of various ages continued unabated until the Campanian. Cretaceous strata are built on a distinctive and characteristic Upper Triassic massive dominantly shelf-related clastic deposits, with minor, geographically- volcanic succession (basalts of the Karmutsen Formation and restricted shallow-marine to subaerial(?) Upper Cretaceous volcanic equivalents), possibly erupted onto pre-existing oceanic basement rocks and deeper-water, slope turbidite facies (Haggart, 1991). (Jones et al., 1977). On Queen Charlotte Islands, these oceanic Calcareous concretions are found at numerous levels in the strati- basalts are succeeded by fringing reef carbonates and deeper water graphic succession; these often contain well-preserved fossil mate- calcareous clastic facies of the Upper Triassic to lowermost Jurassic rials, especially in Santonian and Campanian deposits. Kunga Group (Fig. 2) (see Lewis et al., 1991). Overlying, Lower Correlation of Cretaceous successions of Queen Charlotte Islands Jurassic clastic-rich sedimentary strata of the Maude Group reflect has relied principally on ammonites and other molluscan fossil deposition at some distance from active volcanic activity. By Middle groups (McLearn, 1972; Jeletzky, 1970a, 1977; Haggart, 1991, 1995; to early Late Jurassic time, the locus of magmatism occupied the Haggart and Higgs, 1989), although recent studies of radiolarian Queen Charlotte Islands region; Yakoun and Moresby groups faunas (Haggart and Carter, 1993; Carter and Haggart, 2006)have preserve extensive active arc volcanic and associated epiclastic demonstrated the correlation potential of this fossil group, espe- rocks, respectively, in geographic and temporal association with cially for poorly-fossiliferous deep-water strata of the islands. widespread plutonism. Middle to Late Jurassic magmatic activity Paleogene plutonic rocks are distributed widely on Queen may reflect the initiation of subduction in the region (Lewis and Charlotte Islands (Haggart, 2004) and may document final amal- Ross, 1989; Thompson et al., 1991; Lewis et al., 1991). gamation of Wrangellia terrane with North America (Lewis et al., The Cretaceous stratigraphic succession of Queen Charlotte 1991), although this is by no means established. Subsequently, the Islands records a prolonged period of basin subsidence and sediment Mio-Pliocene Masset Formation represents widespread volcanic activity that accompanied regional extension, and initiated Queen Charlotte Islands’ modern trans-tensional setting (Hickson, 1991).

3. Lithostratigraphy

The stratigraphic succession at Lawn Hill is exposed in a geographically-restricted (w 250 m long) outcrop in the intertidal region on the east coast of Graham Island, Queen Charlotte Islands (Fig. 1; NTS 103G/05: Lawnhill 1:50,000-scale topographic map). The Lawn Hill outcrop is an outlier of Cretaceous rocks on the east side of the Sandspit fault (Fig. 1) and comprises the easternmost outcrop of the informally named Tarundl formation (Haggart, 2002), the youngest unit of the Lower-Upper Cretaceous Queen Charlotte Group (Haggart, 1991) found on Queen Charlotte Islands (Fig. 2). The Tarundl formation has limited geographic distribution across central Queen Charlotte Islands and includes strata from Santonian through Campanian (Haggart and Higgs, 1989; Haggart, 1991, 2002, 2004). The Cretaceous strata at Lawn Hill dip gently to the south and include approximately 60 m of silty mudstone and muddy silt- stone hosting calcareous concretions (Fig. 3). The exposures are not continuous and are generally covered with cobbles and small boulders, the arrangement of which varies from year to year, depending on storm activity. Section thickness was determined using a metal tape and accounting for stratigraphic dip. The base of the section, on the north side of the outcrop, is not seen and is presumed to be faulted. Similarly, the top of the section is cut off by feeder dikes to Neogene volcanic deposits which are inferred to unconformably overlie the Cretaceous strata at Lawn Hill, based on adjacent exposures on Graham Island just above the intertidal zone (Haggart, 2004). The Cretaceous strata are homogeneous in composition and lack distinctive marker beds. Fossils are common throughout the section, both in the matrix as well as in large (w 0.5–1 m) and elongate calcareous concretions, and include molluscs, crustaceans, and wood. Fossils are generally fragmen- tary, both in the matrix and in concretions, but visually-uncom- pacted. Early diagenetic concretions are sometimes marked by doubly-deformed shale laminae draping both concretion tops and bottoms. The Lawn Hill Cretaceous strata are faulted locally and contorted on a sub-outcrop scale. Regionally, the Sandspit fault, striking approximately 140 azimuth, crosses the shoreline of Graham Fig. 2. Mesozoic and Tertiary stratigraphic succession of Queen Charlotte Islands; FM/ Island approximately 10 km south of the Lawn Hill exposure fm ¼ Formation/formation, L ¼ level of Lawn Hill stratigraphic section. (Sutherland Brown, 1968; Haggart, 2004). Multiple splays of this 942 J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951

Fig. 3. Stratigraphic section of Tarundl formation exposed at Lawn Hill, Graham Island, Queen Charlotte Islands, showing levels of fossil collections and paleomagnetic sampling. Fossil locality details available from senior author or Chief of Paleontology, Geological Survey of Canada, Calgary, Alberta. PM ¼ Paleomag Sample [No.], m ¼ meters above base of section. regional-scale fault separate exposures of older, Jurassic and the chlorite replacement typical elsewhere on Queen Charlotte Cretaceous rocks on the west from dominantly Miocene volcani- Islands. clastic strata to the east. Recognizable movement on the Sandspit Fossils found in the Tarundl formation at Lawn Hill preserve fault is primarily east side-down, with throw of hundreds to original aragonite shell material and display iridescent lustre, often thousands of meters (Sutherland Brown, 1968; Yorath and Chase, (but not always) characteristic of organic macromolecules incor- 1981). As a possible consequence of its hanging-wall block affinity, porated systematically into a biomineralized shell matrix. Since the the Tarundl formation exposure at Lawn Hill appears to have near-surface structural inversion of aragonite to calcite proceeds at escaped the thermochemical alteration that pervasively affects low temperature (<100 C), and since fluid exchange alters shell Cretaceous strata in the footwall block (Haggart and Verosub, 1994). matrix proteins and destroys iridescence, aragonitic, iridescent In addition, Mesozoic organic-rich strata exposed on Queen fossils are recognized as markers of locally and regionally unaltered Charlotte Islands are generally overmature (Vellutini and Bustin, outcrops suitable for study in areas of otherwise remagnetized 1991) and most Jurassic and Cretaceous fossil materials from Queen sedimentary (Filmer and Kirschvink, 1989; Ward et al., 1997). Charlotte Islands are altered to black calcite, reflecting thermal Despite this rule-of-thumb, the ‘‘biomineral alteration’’ test is not alteration effects likely associated with Jurassic or Eocene pluton a paleomagnetic field test that provides a direct constraint on the emplacement. Local replacement of shell aragonite by (Mg, Fe)-rich character of remanent magnetization, and normal-polarity viscous chlorite at many localities suggests penetrative chemical mobili- (partial thermal) remanent overprints plague similarly low-grade zation and mineral replacement by fluids passing through wide- sedimentary rocks of similar lihology throughout the Insular spread Upper Triassic Karmutsen Formation basalts (Haggart and superterrane (e.g. Enkin et al., 2001; Kim and Kodama, 2004). Bustin, 1999). This diagenetic alteration could have accompanied post-Eocene extension and exhumation along low-angle normal 4. Molluscan biostratigraphy faults: Eocene and Oligocene volcanic stocks tilt consistently by w11–16 to the north (Lewis and Ross, 1991; Wynne et al., 1992; Representative examples of the Lawn Hill Cretaceous fauna are Irving et al., 2000). Significantly, Cretaceous exposures at Lawn Hill shown in Figs. 4 and 5 and the stratigraphic distribution of are geographically distant from surface exposures of the Karmutsen important taxa is summarized in Fig. 3. Although the molluscan Formation, and Tarundl formation strata do not show evidence of fauna is not especially diverse, it does contain important J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951 943

Fig. 4. Fossils from the Tarundl formation at Lawn Hill, Queen Charlotte Islands; all fossils 1and coated with ammonium chloride before photography. A–C. Gaudryceras den- manense Whiteaves, 1901; A, B. GSC No. 132348, GSC Loc. C-304212, A Latex peel of external mold of inner part of umbilicus, right flank; B. Lateral view of right flank; C. GSC No. 132349, GSC Loc. C-304212 (cf. Gaudryceras tenuiliratum Yabe, 1902); D, E. Zelandites sp. juv.; GSC No. 132350, GSC Loc. C-304212; F. Anagaudryceras politissimum (Kossmat, 1895); GSC No. 132351, GSC Loc. C-304212; G–I. Damesites sp. cf. sugata (Forbes, 1846); GSC No. 132352, GSC Loc. C-304212; Figure G shows flank of outer whorl, figures H and I show the inner whorl; J. Solenoceras sp. cf. mexicanum Anderson, 1958; GSC No. 132353, GSC Loc. C-304209. biostratigraphic and biogeographic elements. The section at Lawn Damesites sp. cf. sugata (Forbes, 1846)(Fig. 4G–I), Gaudryceras Hill was previously considered to represent the lower Campanian denmanense Whiteaves, 1901 (Fig. 4A–C), Anagaudryceras polit- Submortoniceras chicoense Zone, based on a poorly-preserved issimum (Kossmat, 1895)(Fig. 4F), Neophylloceras sp., Nostoceras ammonite fragment identified as Submortoniceras chicoense (Trask, hornbyense (Whiteaves, 1895) (Fig. 5C, D), Diplomoceras sp. cf. ten- 1856)(Haggart, 1995). However, new collections of better- uisulcatus (Forbes, 1846)(Fig. 5E), Solenoceras sp. cf. mexicanum preserved fossil materials have subsequently shown that this Anderson, 1958 (Fig. 4J), Zelandites sp. (Fig. 4D, E), and Baculites specimen is better assigned to the ammonite Pachydiscus suciaensis sp. cf. occidentalis Meek, 1862 (Fig. 5F). Also found in the section are (Meek, 1862)(Fig. 5A, B). In addition, a number of additional the bivalves Cordiceramus ? sp. (Fig. 5H) and Inoceramus sp. cf. ammonite taxa are now known from the Lawn Hill site, including vancouverensis Shumard, 1859 (Fig. 5G). 944 J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951

Fig. 5. Fossils from the Tarundl formation at Lawn Hill, Queen Charlotte Islands; all fossils 1and coated with ammonium chloride before photography. A, B. Pachydiscus suciaensis (Meek, 1862); GSC No. 132354, GSC Loc. C-304209; C, D. Nostoceras hornbyense (Whiteaves, 1895); C. GSC No. 132355, GSC Loc. C-304209, retroversal body chamber hook; D. GSC No. 132356, GSC Loc. C-304210, retroversal body chamber hook; E. Diplomoceras sp. cf. tenuisulcatus (Forbes, 1846); GSC No. 132357, GSC Loc. C-304212; F. Baculites sp. cf. occidentalis Meek, 1862; GSC No. 132358, GSC Loc. C-304214; G. Inoceramus sp. cf. vancouverensis Shumard, 1859; GSC No. 132359, GSC Loc. C-304209; H. Cordiceramus ? sp.; GSC No. 132360, GSC Loc. C-304210.

5. Paleomagnetism IRM indicates a median coercivity of approximately 40 mT; together, these parameters suggest the presence of detrital magnetite, tita- Twenty-seven oriented paleomagnetic sample cores were dril- nomagnetite, and/or biogenic magnetite (Fig. 6). AF demagnetization led in twenty-five distinct concretions belonging to seven strati- of anhysteretic remanent magnetization (ARM) reduces saturation graphic levels spaced through wsixty meters of exposed section. All IRM to zero at a marginally higher field strength than AF of IRM, samples underwent low alternating-field and progressive thermal suggesting the presence of single-domain crystals capable of demagnetization in a low-field (<10 nT) shielded furnace, and retaining primary magnetizations against low thermal- and viscous- progressively decaying remanence was measured on a three-axis remagnetizing effects for significant periods of time (Cisowski,1981). SQuID magnetometer with ambient field shielded to a background In directional experiments, AF demagnetization up to 10 mT in level of generally less than 100 nT and less than 5 nT in the 1.0 mT to 1.25 mT steps removes low-coercivity components machine’s sense region. Paleo- and rock-magnetic measurements usually accounting for 25–50 % of net natural remanent intensity. were collected using an automated sample-changing system Post-AF magnetization is generally w5 109 Am2. Samples were (Kirschvink et al., 2008) and magnetization directions were thermally demagnetized in closely-spaced steps from 100 C until analyzed using least-squares analysis (Kirschvink, 1980) in the they became unstable, generally between 340 C and 425 C, and software program Paleomag (Jones, 2002). rarely to w 550 C. These elevated unblocking temperatures are For a powdered, representative sample, acquisition of isothermal also consistent with magnetite and/or titanomagnetite as the remanent magnetization (IRM) effectively saturates between 200 magnetization carrier, unstable during thermal demagnetization and 300 mT, and alternating field (AF) demagnetization of saturation during calcination reactions. J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951 945

100 6. Discussion AF of ARM AF of IRM 6.1. Zonal assignment 80 Most of the Lawn Hill molluscan taxa are known from other IRM Acquisition localities along the Pacific coast of North America. Nostoceras 60 hornbyense is found commonly in exposures of the upper Nanaimo Group of British Columbia, especially at Hornby Island where it is associated with Baculites occidentalis, Didymoceras vancouverense, QCHS 68 and Phyllopachyceras forbesianum (Ward, 1978); examples are also 40 0.98 g IRM =3.94e-5 A/m known from southern Alaska (Jones, 1963). Anagaudryceras polit- max issimum and Damesites sugata are also found in the upper Nanaimo

% of maximum intensity Group, commonly in association with Pachydiscus suciaensis (Hag- 20 gart, 1989). The diplomoceratid ammonite Solenoceras mexicanum is known from the Rosario Formation of Baja California (Anderson, 1958), but, to date, representatives of the genus have not been 0 recognized north of California (although the southern Alaskan 1 53050 100 1000 specimen referred to Pseudoxybeloceras? sp. indet. by Jones 1963 Applied Field (mT) (pl. 16, fig. 9) is likely referable to the genus). The Lawn Hill spec-

Fig. 6. Representative rock-magnetic data from Tarundl formation calcareous imen compared herein with S. mexicanum is of smaller size than the concretionary shale. Moderately-interacting ferromagnetic minerals, likely magnetite illustrated Baja examples, although it exhibits similar morphology. and/or titanomagnetite, have median coercivity of w40 mT and mostly saturate The bivalve Inoceramus vancouverensis is a common component of between w200 and w300 mT. A positive modified ‘‘Lowrie-Fuller’’ test with ARM Campanian assemblages of the Nanaimo Group and has also been harder than IRM suggests substantial presence of single-domain particles. Thermal recognized in the Campanian of California (Matsumoto, 1960). unblocking spectra (described in the text) also support a mixture of stable single- domain with multi-domain (viscous-remagnetized) magnetite and/or titanomagnetite The ammonite specimen GSC (Geological Survey of Canada) No. particles. 132349, herein assigned to Gaudryceras denmanense (Fig. 4C), bears strong resemblance to material figured by Jones (1963, pl. 9, pl. 10, figs. 1–3) as Gaudryceras tenuiliratum Yabe; the strong and dense ribbing in the intermediate growth-stage of Jones’ specimens Most samples exhibit a low-coercivity component uniquely stands in contrast to that of typical examples of G. denmanense (cf. removed by alternating field demagnetization (Fig. 7A). The Usher, 1952, pl. 4, figs. 1–2; Haggart, 1989, pl. 8.3, fig. 1). Earlier mean of this component’s in-situ distribution lies near the work on gaudryceratids of the Nanaimo Group led Haggart (1989) present local field direction (23-sample mean at D ¼ 356.4, to synonymize Jones’ materials within G. denmanense. The present I ¼ 76.5 versus present field at D ¼ 22.8,I¼ 77.2 using IGRF coarsely ribbed specimen, found at the same level as more 2000 model coefficients). Many samples also exhibit a north- smoothly-ornamented forms readily assigned to G. denmanense, and moderately-down magnetization of low thermal stability thus illustrates the variability found within single populations of (< 290 C). Similar to both the present-field direction and to Upper Cretaceous gaudryceratids and may have implications for Cenozoic volcanic magnetizations elsewhere on Graham Island taxonomic assignments of gaudryceratids in other regions, as well (Irving et al., 2000), this magnetization is likely a viscous as the specific composition of the genus. remagnetization carried by the largest fraction of magnetite/ Based on the presence of Pachydiscus suciaensis, the strata at titanomagnetite grains. Lawn Hill are broadly referable to the Pachydiscus suciaensis Zone of A third component is poorly expressed. A few samples record an western Canada. Jeletzky (1970a,b) established the Pachydiscus apparently stable endpoint magnetization unblocking above suciaensis Zone for fossiliferous Upper Cretaceous strata of the w290 C with a reversed-polarity direction (Fig. 7C) dissimilar from Pacific slope of Canada containing the zonal index and other taxa, any Tertiary remagnetization. One sample yields an apparently including the heteromorph Nostoceras hornbyense. The Pachydiscus antipodal, north and shallow-down magnetization distinct from suciaensis Zone is well developed in the Nanaimo Group of Van- the lower-temperature viscous overprint (Fig. 7B). couver Island where it has been interpreted previously to have Other samples yield remagnetization arcs trending toward the a late Campanian to possibly early Maastrichtian age (Jeletzky, south and upward-directed reversed-polarity magnetization 1970b; Ward, 1978; Haggart, 1995; w 77–71 Ma); the zone has not (Fig. 7D), but due to inherent ambiguities intersecting remagneti- been recognized elsewhere in British Columbia prior to this report. zation circle arc constraints absent sufficient reliable endpoint data Ward (1978, table 1) furthermore suggested that strata of the (Halls, 1978), it is not possible to determine a mean magnetization P. suciaensis Zone on Vancouver Island and adjacent regions con- direction with confidence, even though the polarity-call is clear. taining the heteromorph Nostoceras hornbyense and other ammo- Furthermore, the viscous remagnetization is so pervasive that nite taxa comprise a local zonule within the upper part of the ancient normal-polarity magnetizations may be indistinct from P. suciaensis Zone. Nostoceras hornbyense and Pachydiscus suciaensis higher-temperature tails of viscous overprints, although at least both occur in the Lawn Hill section at GSC Loc. 304209, approxi- one sample yields an unquestionably distinct normal-field direc- mately 4 meters above the base of the section (Fig. 3); neither taxon tion (Fig. 7B). is recognized higher in the stratigraphic section at Lawn Hill. Collectively, these data nonetheless clearly indicate at least Based on the new recognition of the Nostoceras hornbyense impersistent recording of reversed-polarity magnetization. fauna on Queen Charlotte Islands, and the previous identification Because latest Campanian time is dominated by normal of N. hornbyense in southern Alaska (Jones, 1963), we propose that polarity with the exception of three short subchrons in C32, the N. hornbyense zonule be elevated to the status of a formal the paleomagnetism of Tarundl formation shale constrains its faunal zone for the Pacific coast region of western Canada, depositional age to either 73–72 Ma or else ca. 71 Ma (Ogg stratigraphically succeeding the Pachydiscus suciaensis Zone et al., 2004). (Fig. 8); the stratigraphic section at Lawn Hill is thus assigned to 946 J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951

Geographic A LH coordinates

300 C B 390 C

250 C D LH LH

QCHS 240 QCHS 53 Tilt-corrected coordinates Tilt-corrected coordinates 210 C

NRM 125 C

125 - 190 C 250 C

NRM

NRM 260 C 160 C AF <10 mT 290 C

175 C Tilt-corrected coordinates QCHS 263 LH 345 C 225 C UH

C 290 - 520 C

Fig. 7. Paleomagnetic characterization of Cretaceous strata at Lawn Hill on equal-area stereonet diagrams. A. In-situ, well-defined low-coercivity overprints removed by alternating- field demagnetization to 10 mT. 95% confidence interval indicated, overlapping the present field direction (asterisk). B. Normal-polarity end-point magnetization distinct from present-field viscous overprint. C. Well-defined, reversed-polarity endpoint distinct from present-field viscous overprint, approximately antipodal to normal-polarity end-point magnetization in B and dissimilar from any plausible Tertiary remagnetization. D. Poorly-defined suggestion of reversed polarity, indicated by remagnetization arc trending away from present-field direction at ever-higher temperature steps. Subsequent thermal steps yielded unstable magnetization behaviour, presumably associated with magnetic mineral alteration associated with calcination reactions. LH ¼ Lower Hemisphere; UH ¼ Upper Hemisphere.

the new Nostoceras hornbyense Zone. The base of the new faunal The Nostoceras hornbyense Zone is the youngest ammonite zone on Queen Charlotte Islands is located ca. 4 meters above the faunal zone recognized to date in the Cretaceous of Pacific coast base of the exposed section at Lawn Hill (ca. UTM Grid Reference Canada. Exposures of the zone on Hornby Island (Fig. 1) constitute 306475E, 5923050N, Zone 9; NAD 27), at the first occurrence in the stratigraphically-highest fossiliferous strata within the North- the section of N. hornbyense. The upper limit of the zone is not umberland Formation of the Nanaimo Group. Higher Nanaimo seen, but continues to the top of the exposed section (ca. UTM Group strata of the Spray Formation on Hornby Island are inferred Grid Reference 306450E, 5922800N, Zone 9; NAD 27), which is also to be Late Cretaceous in age (Jeletzky, 1970b; Ward, 1978), but, cut by a Neogene dike. to date, these submarine-fan deposits have not produced diag- nostic faunal elements. J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951 947

southern Alaska (Jones, 1963), and the upper Campanian of Nigeria Stage (Ma) Ward (1978) This paper (Zaborski, 1985) and Angola (Howarth, 1965). Similarly, the closely comparable Didymoceras awajiense is known from upper Campa- nian deposits of Japan (Morozumi, 1985). Unfortunately, the ino- No faunas known L No faunas known ceramid bivalves present in the Lawn Hill assemblage must be considered non-diagnostic, as they are only compared tentatively ? ?

Maastrichtian 70.6 N. hornbyense with other known taxa from the west coast of North America. Pachydiscus zonule Nostoceras hornbyense Interestingly, the ammonite Pachydiscus neubergicus has not yet suciaensis been reported from Upper Cretaceous deposits of west coast ? ? Pachydiscus suciaensis Canada and the United States. In the western Pacific region, this Metaplacenticeras U Metaplacenticeras worldwide index of the lower Maastrichtian (Kennedy and Sum- cf. pacificum cf. pacificum mesberger, 1986; Christensen et al., 2000) is known from both Hoplitoplacenticeras Hoplitoplacenticeras Australia (Henderson and McNamara, 1985) and Far East Russia vancouverense vancouverense (Vereshchagin et al., 1965; Yazykova, 1994, 2004; Zonova et al.,

Campanian 1993). We argue that the lack of this widespread marker in both the Baculites chicoensis Nostoceras hornbyense and underlying Pachydiscus suciaensis zones, L Baculites chicoensis although certainly not definitive, is additional evidence that these Sphenoceramus molluscan faunas are of late Campanian age and do not extend into 83.5 schmidti Sphenoceramus the early Maastrichtian. Eubostrychoceras ex gr. schmidti The late Campanian age of the Nostoceras hornbyense Zone at

Sant. elongatum Lawn Hill is also supported by radiolarian microfossils (Fig. 9). Calcareous nodules collected from near the top of the Lawn Hill Fig. 8. Campanian-Maastrichtian molluscan biostratigraphic zonation for western section yielded the first Campanian radiolarians identified from Canada proposed by Ward (1978) and that favored here. Absolute ages after Ogg et al. (2004). Sant. ¼ Santonian. western Canada. Included are Porodiscus cretaceus Campbell & Clark, Pseudoaulophacus cf. floresensis Pessagno, Stichomitra carne- giensis (Campbell & Clark), S. cf. livermorensis (Campbell & Clark), The N. hornbyense Zone of western Canada is also broadly and S. sp. A, all from GSC Loc. C-210839. correlative with the Pachydiscus kamishakensis Zone of southern Porodiscus cretaceus, Stichomitra carnegiensis, and S. liver- Alaska (Jones, 1963), which has been assigned to the uppermost morensis were described by Campbell and Clark (1944) from the top Campanian to lowermost Maastrichtian (Jones, 1963) and contains of the Cretaceous series (Corral Hollow shale) of the Tesla Quad- similar taxonomic components, including N. hornbyense. rangle east of San Francisco, California. An ammonite found with this fauna was reported as Lytoceras (Tetragonites) aff. epigonus,now 6.2. Age assigned to the Campanian species Tetragonites popetensis (Mat- sumoto, 1959). Pseudoaulophacus floresensis was described from The age of the Pachydiscus suciaensis Zone, including strata of lower Campanian strata in Puerto Rico (Pessagno, 1963), and is the new Nostoceras hornbyense Zone, was previously interpreted common in the lower to upper Campanian Crucella espartoensis as latest Campanian to earliest Maastrichtian (Jeletzky, 1970b), Zone of the Great Valley sequence in California (Pessagno, 1976). based on foraminiferal data from the well exposed succession of Stichomitra sp. A figured herein appears identical to a species the upper Nanaimo Group on Hornby Island (McGugan, 1979); from Shikoku, Japan identified by Hashimoto and Ishida (1997, pl. 3, this interpretation for the age of the zone has been followed fig. 10) as S. carnegiensis. This species is included in the Amphi- subsequently by most workers (e.g. Ward, 1978; Haggart, 1989; pyndax pseudoconulus Assemblage Zone of Japan, which the England and Hiscott, 1992; Mustard, 1994). Although precise authors indicate is upper Campanian based on associated Inocer- correlation of the North Pacific Upper Cretaceous sequences with amus balticus and Pravitoceras sigmoidale. Both the Japanese spec- European international stratotypes is problematic, due to limited imen and ours differ from Stichomitra carnegiensis in having fewer numbers of shared taxa and long ranges of a number of species, chambers and a much simpler pattern of ornamentation on distal several of the ammonite taxa present in the Nostoceras horn- chambers and are probably a different species; nevertheless the age byense Zone at Lawn Hill have a restricted stratigraphic range and, assignment is pertinent. we argue, serve to establish a late Campanian age for the zone Based on the evidence presented above, the radiolarian (w 75–70 Ma). assemblage from Lawn Hill is probably late Campanian in age and Haggart (1989) showed that Gaudryceras denmanense is restricted illustrates the wide distribution of radiolarians in Panthalassa to strata of late Campanian age in the upper part of the Nanaimo during the Late Cretaceous. Group of the Vancouver Island area. In addition, the diplomoceratid The age for the Lawn Hill Tarundl formation section suggested by ammonite Solenoceras has been collected from the Lawn Hill radiolarians thus supports the age assignment based on molluscs. The succession. Examples of this genus are rare from west coast of North late Campanian age indicated by molluscs and radiolarians also America, but are common in middle and, especially upper Campanian supports placement of the Lawn Hill section within one of the short strata of other regions, including the US Western Interior (Scott and reversed subchrons within or adjacent to Chron C32 (Ogg et al., 2004). Cobban,1986; Larson et al.,1997; Kennedy et al., 2000) and Gulf Coast We prefer correlation of the Lawn Hill section with the strati- (Stephenson,1941; Cobban and Kennedy, 1994), Europe (Ku¨ chler and graphically-highest of these subchrons as the age of the Nostoceras Odin, 2001; Naidin, 1974)andtheMiddleEast(Lewy, 1969), Japan hornbyense Zone at Lawn Hill is assigned to the high Campanian. (Tanaka, 1980; Matsumoto and Morozumi, 1980; Morozumi, 1985), Given their late Campanian age, the Tarundl formation expo- and Chile (Hu¨ nicken et al., 1975). sures at Lawn Hill represent the youngest Cretaceous strata known The zonal namesake of the Nostoceras hornbyense Zone is also on Queen Charlotte Islands. Indeed, the next older Cretaceous fauna known from upper Campanian deposits in other regions, including known from Queen Charlotte Islands, also from the Tarundl the US Gulf Coast (Cobban and Kennedy, 1994). Material compared formation but exposed in the western Skidegate Inlet area, is of late with N. hornbyense is known from the upper Campanian of Santonian to early Campanian age (Haggart and Higgs, 1989). 948 J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951

Fig. 9. Radiolarians from upper Campanian beds at Lawn Hill, Queen Charlotte Islands; all specimens from GSC loc. C-210839. Length of scale bar ¼ 100 micrometres (mm) for each illustration. A. Porodiscus cretaceus Campbell & Clark, GSC No. 132361. B. Pseudoaulophacus cf. floresensis Pessagno, GSC No. 132362. C. Stichomitra carnegiensis (Campbell & Clark), GSC No. 132363. D. Stichomitra sp. A., GSC No. 132364. E. Stichomitra cf. livermorensis (Campbell & Clark), GSC No. 132365.

7. Conclusions Group of southwestern British Columbia. Based on the new data demonstrating that N. hornbyense is more widely distributed along We have recognized the Nostoceras hornbyense zonule of the the west coast of North America than previously considered, we Pachydiscus suciaensis Zone of the west coast North American Upper have proposed that this zonule be raised to zonal status. So far as Cretaceous in strata on Queen Charlotte Islands, British Columbia. A known, the N. hornbyense Zone is restricted to the upper Campa- stratigraphic section exposed in the intertidal region at Lawn Hill, on nian along the west coast of North America, as diagnostic fossils of the east coast of the islands, includes both N. hornbyense and P. the lower Maastrichtian, such as Pachydiscus neubergicus and its suciaensis, as well as a diverse assemblage of ammonites and ino- equivalents, have yet to be found in association with the zonal ceramids that are assigned a late Campanian age. Radiolarians index. As well, the highest fossiliferous exposures of the North- associated with the mollusc fossils also support a late Campanian umberland Formation at Hornby Island, British Columbia, which age. Calcareous concretions found in the section exhibit reversed- are rich with N. hornbyense, can be correlated with the uppermost polarity magnetization which we correlate with Chron 32r. Campanian, rather than the lower Maastrichtian as postulated The N. hornbyense Zonule of the P. suciaensis Zone was estab- previously (McGugan in Jeletzky 1970b); however, strati- lished by Ward (1978), based on limited exposures in the Nanaimo graphically-higher strata on Hornby Island (Geoffrey, Spray, and J.W. Haggart et al. / Cretaceous Research 30 (2009) 939–951 949

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Zaborski, P.M.P.,1985. Upper Cretaceous ammonites from the Calabar region, south-east GSC Loc. C-187385. Zone 9, 306475E, 5923025N; near base of exposed Nigeria. Bulletin of the British Museum (Natural History), Geology Series 39, 1–72. stratigraphic section; Coll. J.W. Haggart, 1990. Zonova, T.D., Kazinskova, L.I., Yazykova, E.A. (Eds.), 1993. Atlas Rukovodyashchikh GSC Loc. C-304209. 306475E, 5923025N; 4.2 m above base of exposed stratigraphic Grupp Melovoi Fauny Sakhalina [Atlas of the main groups of the Cretaceous section;Coll.J.W.Haggart,1998. fauna from Sakhalin]. Vsesoyuznyi Ordena Lenina Nauchno-Issledovatelskii GSC Loc. C-304210. 306475E, 5923025N; 8.5 m above base of exposed Geologicheskii Institut imeni A.P. Karpinskogo (VSEGEI), Izdatel’stvo Nedra, St. stratigraphic section; Coll. J.W. Haggart, 1998. Petersburg 327 p., 107 pls. (In Russian). GSC Loc. C-304212. 306475E, 5923025N; 42.0 m above base of exposed stratigraphic section; Coll. J.W. Haggart, 1998. GSC Loc. C-304213. 306475E, 5923025N; 42.0 m above base of exposed stratigraphic Appendix. Fossil localities section;Coll.J.W.Haggart,1998. GSC Loc. C-304214. 306475E, 5923025N; 49.5 m above base of exposed Data from Geological Survey of Canada Paleontological Database, Vancouver, stratigraphic section; Coll. J.W. Haggart, 1998. British Columbia. All fossil localities are those of Geological Survey of Canada (GSC) GSC Loc. C-210839. 53 25.430N, 131 54.770W; near top of exposed stratigraphic and are located on NTS Topographic Map 103G/05 (Lawnhill). section; Coll. E.S. Carter, 1993.