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Three-dimensionally phosphatized, spherical fossils, interpreted as metazoan eggs and embryos on the basis of taphonomic features and cleavage patterns, are reported for the first time from the Cambrian of North America. These microfossils occur with a phosphatized biota of skeletonized fossils, including specimens indicative of the earliest Cambrian AnabaritesProtohertzina Zone in the Wernecke Mountains of eastern Yukon Territory, northwestern Canada. They range in size from 0.25 mm to more than 1.0 mm in diameter and can be referred to two genera, Olivooides Qian, 1977 and Archaeooides Qian, 1977. The North American discovery extends the biogeographic range of earliest Cambrian eggs and embryos from coeval successions in China and Siberia, suggesting a wide geographic distribution of these taxa, and emphasizes the crucial role of local environmental and taphonomic conditions in preserving this phosphatic window into the record of early animal evolution. In addition to previously reported taxa, the phosphatized biota also include indeterminate spheroids, fused clusters of Protohertzina siciformis Missarzhevsky, 1973, the enigmatic rodlike fossil Zhejiangorhabdion comptum Yue and Zhao, 1993, phosphatized fossils, including Paradoxiconus typicalis Qian et al., 2001, protoconularid Carinachites sp., and phosphatic tubes assigned to Hyolithellus cf. H. isiticus Missarzhevsky, 1969, cf. Pseudorthotheca sp., and ?Rugatotheca sp.


Discovery of phosphatized animal embryos in various developmental stages in Cambrian (Zhang and Pratt, 1994; Bengtson and Yue, 1997; Kouchinsky et al., 1999; Yue and Bengtson, 1999; Dong et al., 2004) and Neoproterozoic rocks (Xiao et al., 1998, 2000; Xiao and Knoll, 1999, 2000; Yin et al., 2004) has dramatically advanced knowledge of a previously missing part of the metazoan record. Further exploration of the phosphatization taphonomic window (Brasier, 1990; Dzik, 1994) in the Neoproterozoic–Cambrian transition will provide critical paleontological data to test various hypotheses about the tempo and mode of early animal evolution (Wray et al., 1996; Ayala et al., 1998; Knoll and Carroll, 1999; Valentine, 2002). New discoveries of these fossils and co-occuring phosphatic microfossils will offer more insights into the morphology, taphonomy, and biogeography of the earliest animals.

All previous reports of phosphatized eggs and embryos of early animals have been from Asia. We report for the first time an earliest Cambrian, Laurentian occurrence of three-dimensionally phosphatized globular microfossils interpreted as animal eggs and embryos from northwestern Canada. In addition, a number of phosphatized shelly microfossils with three-dimensional detail are described. This diverse assemblage adds another view into the evolutionarily dynamic interval of the Proterozoic–Phanerozoic transition.

geology and age of fossil locality

Carbonate rocks sampled for phosphatic microfossils are from a remote ridge in the Wernecke Mountains, Yukon Territory, northwestern Canada (Fig. 1.1). The upper boundary of the Neoproterozoic Windermere Supergroup in the study area lies at the top of the karsted and massively dolomitized shallow-water carbonates of the Risky Formation (Pyle et al., 2004). Lowermost Cambrian sediments are carbonates of the Ingta Formation (Fig. 1.2), specifically thin-bedded, parted to nodular limestones with attributes indicating a mid- to outer-ramp paleoenvironmental setting. This limestone grades up into and is topped by a prominent phosphatic hardground complex, that is in turn overlain by thick, black shale that coarsens upward into hummocky cross-stratified sandstones of the Vampire Formation (Osborne et al., 1986). The phosphatic interval is a rudstone of tabular lime mudstone clasts with all the attributes of storm deposition (cf. Mount and Kidder, 1993), surrounded by a matrix rich in small shelly fossils. These tempestites are capped by a 10–20 cm thick phosphate hardground that forms a rind on top of the clast rosettes and coats pebbles as much as 40 cm below. This phosphatic horizon is interpreted as a maximum flooding surface (cf. Loutit et al., 1988). Material for this study comes from samples collected within the uppermost 70 cm of the Ingta Formation (9 m thick total).

Nowlan et al. (1985) described small shelly fossils, including Anabarites trisulcatus Missarzhevsky, 1969 and Protohertzina anabarica Missarzhevsky, 1973, from the phosphatized limestone unit that was referred to as a basal unit of the Vampire Formation before the Ingta Formation was named formally. Pyle et al. (2004) reassigned this carbonate unit to the Ingta Formation, which lies below the siliciclastic-dominated Vampire Formation in correlative strata of the Mackenzie Mountains. Samples collected from the phosphatic limestone horizon yielded abundant small shelly fossils, including additional specimens of Anabarites Missarzhevsky, 1969 and Protohertzina Missarzhevsky, 1973. This level can be correlated with the oldest shelly fossil zone that marks the base of the basal Cambrian Nemakit–Daldynian Stage in Siberia (Khomentovsky and Karlova, 1993) and the Meishucunian Stage in South China (Qian and Bengtson, 1989). Complex trace fossils, including Treptichnus pedum Bahde et al., 1997, Rusophycus avalonensis Crimes and Anderson, 1985, and Cruziana sp. d'Orbigny, 1842, indicative of a subtrilobite Cambrian age, occur at the base of the overlying Vampire Formation (Fritz et al., 1983; Nowlan et al., 1985; Narbonne and Aitken, 1995) (Fig. 1.2).

materials and methods

The fossil locality is Section 8E of Nowlan et al. (1985), reexamined as Section D1 by Pyle et al. (2004). Specimens were extracted from archived reconnaissance samples collected for small shelly fossils in 1982 and 1984 and from more detailed collections made during 2002. Samples of the phosphatized limestone come from a 70 cm interval in a unit assigned to the Ingta Formation (Fig. 1.2). After dissolution of samples in 10% acetic acid, phosphatized specimens were manually isolated from the insoluble residue and sorted under a binocular microscope. Samples yielded a total of more than 5,000 globular specimens and thousands of small shelly fossils from all standard sieve fractions ranging from less than 150 μm to more than 850 μm. Images were captured using a JEOL 6301F Field Emission Scanning Electron Microscope. Illustrated specimens are housed in the National Type Repository in the Geological Survey of Canada (GSC), Ottawa, Ontario.

systematic paleontology

Identification of spherical microfossils as spawned eggs and early developmental stages of animal embryos is based on the nature of surficial and internal features preserved by three-dimensional phosphatization, particularly taphonomic evidence that the spheres were hollow with a pliable, organic membrane (see discussions within each taxa). Systematics of spherical fossils have been both clarified and complicated by the discovery of internal details of some fossils such as the stellate embryos of Olivooides Qian, 1977 (Bengtson and Yue, 1997) and germ band formation in Pseudooides Qian, 1977 (Steiner et al., 2004a). Preservational differences among reported occurrences of globular fossils have obscured structural and functional interpretations of spheres that lack distinct embryonic features and have also hampered systematics of these genera. In this present study, where few internal details were evident, form taxonomy is used. Smooth specimens are comparable to Olivooides and those with pustulose ornamentation are assigned to the genus Archaeooides Qian, 1977. Li and Qian (1999) reviewed the research history of spheroidal fossils. The following describes the phosphatized biota grouped into spherical microfossils, anabaritids and protoconodonts, rodlike fossils, pyramidal, conical, and bulbous fossils, carinachitids, and tubes and plates.

Spherical Microfossils

Genus Olivooides Qian, 1977

Type species

Olivooides multisulcatus Qian, 1977.

Original diagnosis

Spheroidal, egglike, wide-elliptical or spindlelike shell, 0.33–1.7 mm in diameter, with a hollow interior. Shell thickness uneven, organic. Shell surface smooth, with depressions and furrows (translated from Qian, 1977).


Lower Cambrian, China (Qian, 1977; review of stratigraphic distribution by Xing et al., 1984), India (Bhatt et al., 1985; Brasier and Singh, 1987; Kumar et al., 1987), and Siberia (Yue and Bengtson, 1999).

Olivooides sp. Figures 2, 3


Phosphatized, spherical to elliptical globules ranging from less than 0.4 mm to greater than 1.0 mm in diameter. Specimens have smooth, spherical envelope (Fig. 2.1) or indented, buckled, collapsed, or deflated envelopes (Fig. 2.2–2.5, 2.9, 2.10). Distinct size groupings represented by spheres approximately 0.6–0.7 mm wide (Fig. 2.1–2.4, 2.6, 2.9, 2.10), and 0.4 mm wide (Fig. 2.7, 2.8). Largest specimens are greater than 1 mm long and are elliptical (Fig. 2.5). Envelope typically 5 μm thick (Fig. 2.9) but can be thicker due to infilling by phosphate (Fig. 2.11) and phosphatic encrustation (Fig. 2.12, 2.15, 2.16). Two completely exposed specimens each have two hemispherical internal bodies (Fig. 2.6, 2.8). Where envelope is partially broken on one specimen, surface indentations appear to follow boundaries of underlying internal bodies (Fig. 2.9, arrows). Regular patterning of indentations occurs on smooth envelopes (Fig. 2.2, 2.3, 2.10). Hollow specimens (Fig. 2.12, 2.15, 2.16) show variable degrees of wall thickening, are partially infilled with phosphate, and some contain filaments coated by spherulitic botryoidal apatite (Fig. 2.13). Filaments in cross section have a core 10 μm in diameter, thickened to 22 μm in diameter by spherulitic coating (Fig. 2.14). Large sphere (Fig. 2.15) is 0.9 mm in diameter, of which interior space has diameter of 580 μm and walls thickened to 180 μm by isopachous apatite. One shrunken internal body is 185 μm across and hollow, coated and suspended by phophatic filaments (Fig. 2.15). Second large, hollow sphere is 895 μm in diameter (Fig. 2.16), with walls thickened to about 30 μm in 5 layers (Fig. 2.17, 2.18), the innermost layer formed of botryoidal phosphate. Inner body in this specimen may simply be a body of botryoidal phosphate that irregularly coats the interior of the sphere. Several specimens bear centrally located sulcus on one side (Fig. 3.1, 3.2). In cross-sectional view (Fig. 3.3), specimens are hollow and infilled by radial fibrous apatite crystals (Fig. 3.3, arrow; 3.4).


Lower Cambrian, Wernecke Mountains, Yukon Territory, Canada.


Several ontogenetic stages of stellate and striate embryos described by Bengtson and Yue (1997) suggest cnidarian affinities for Olivooides multisulcatus. The present material does not have the stellate and striate structures of O. multisulcatus, but it does resemble smooth spheres described by Qian (1977) as Olivooides. Identification at species level requires postembryonic features that were not preserved in the present material. Developmental stages beyond the two-celled stage were not present, thus the Wernecke material is referred to as Olivooides sp. Among the thousands of globular specimens recovered, spheres have several size groupings which suggest that more than one taxon may be represented. External features indicate an original flexibility to the membrane which supports the biological nature of these spheres and indicates that postmortem infoldings formed prior to phosphatic replacement and encrustation. Buckling of the envelope is a feature exhibited in other Olivooides material (e.g., Yue and Bengtson, 1999, figs. 4, 5), in smooth vesicles of the Duoshanto material (e.g., Xiao and Knoll, 1999, fig. 6e), and in collapsed egg envelopes of Recent copepod eggs (van Waveren, 1993). Regularity of the buckling patterning of the envelope may mirror underlying internal bodies and is similar to a polygonal pattern observed by Kouchinsky et al. (1999) that was interpreted as a hollow blastula stage embryo. Specimens interpreted as two-celled embryos bear a cleavage furrow that approximately divides the sphere into two hemispherical bodies that are interpreted as blastomeres separated by a unipolar furrow (Fig. 2.6, 2.8). Deep sulci on specimens (Fig. 3) could simply be due to compression while the outer membrane was still pliable.

The spherical microfossils, like the co-occurring small shelly components of the biota, were preserved by phosphatization. Calcium phosphate within the spheres and within their envelopes was indicated by qualitative elemental analysis using energy-dispersive X-ray spectrometry. The pliable nature of the envelope indicates secondary, diagenetic phosphatization whereby phosphate replaced soft tissue and/or encrusted the envelope, thus thickening it. The hollow specimens filled with filaments are similar to those illustrated in other phosphatized embryos (e.g., Kouchinsky et al., 1999, fig. 3d; Yue and Bengtson, 1999, fig. 9) and Early Cambrian small shelly fossils (e.g., Conway Morris and Chen, 1992, fig. 7.10). Filaments differ from unbranched tunnels identified as microbial endolithic borings (e.g., fig. 10 in Bengtson et al., 1990). Filaments may instead be a diagenetic feature representing decomposed soft tissue where a filamentous organic structure such as bacteria or fungal hyphae were encrusted by phosphate (Yue and Bengtson, 1999; Xiao and Knoll, 2000). In the Duoshantuo material examined by one of us (SX), where microspherules and filaments are present in abundance, cellular preservation tends to be compromised. This may account for the paucity of preserved blastomere patterns.

Genus Archaeooides Qian, 1977

Type species

Archaeooides granulatus Qian, 1977.

Original diagnosis

Spheroidal, oblate or elliptical spheroidal shell, 0.5–2.5 mm in diameter. Shell wall thin, composed of chitin or phosphate. Shell has hollow interior space. Shell surface ornamented by regularly distributed nodes, closely spaced, some of which contain a tiny hole. Surface of some specimens bears depressions and foldings (translated from Qian, 1977).


Lower Cambrian, Australia (Conway Morris in Bengtson et al., 1990 and discussion of synonymy therein), China (Qian, 1977; Qian and Bengtson, 1989 and references therein), Mongolia (Voronin et al., 1982), Siberia (Sokolov and Zhuraleva, 1983; Val'kov, 1987), Kazakhstan (?=Gaparella porosa Missarzhevsky in Missarzhevsky and Mambetov, 1981), and India (?=Maikhanella sp. Bhatt et al., 1985, although this species is a cap-shaped fossil rather than a sphere and the Tal specimen may be a fragment of Archaeooides).

Archaeooides sp. Figure 4


Phosphatized, subspherical to spherical globules ranging from less than 0.4 mm to greater than 1.5 mm in diameter. Spheres with pustulose surficial ornamentation on outer envelope bear well-developed, regular pattern of protuberances over entire sphere (Fig. 4.1–4.12, 4.16–4.18) or subtle, more irregular pattern (Fig. 4.13–4.15). Similar size range and groupings to smooth spheres, but typically larger specimens (greater than 600 μm in diameter) have most pronounced ornamentation. Specimens are spherical (Fig. 4.1) to subspherical (Fig. 4.9, 4.10) and many have buckled and deflated envelopes (Fig. 4.2, 4.3, 4.5, 4.6, 4.11, 4.18). Broken specimen (Fig. 4.6) reveals a thin, ornate wall (less than 10 μm, Fig. 4.8) enclosing the partially hollow sphere.

Microornament varies from distinct, regularly distributed, raised protuberances that bear a central pore (Fig. 4.1–4.7) to more subtle, nodular ornament (Fig. 4.9–4.18). Protuberances are as high as 15 μm and about 40 μm across (Fig. 4.4, 4.7). Protuberances are preserved as irregular or distinct pustules that range from 15 to 80 μm in diameter. Preservation of ornament varies where pores of pustules are degraded (Fig. 4.1) or may be coated with phosphate where pores are not evident (Fig. 4.9– 4.18). Degradation of outer layer containing pores occurs whereby pustules are preserved only within deflated surfaces (Fig. 4.5).

External features include regular patterns of deflation with one (Fig. 4.3) to two concavities (Fig. 4.5, 4.11, 4.18). One specimen bears an X-shaped furrow on one pole that divides the sphere into at least four bodies (Fig. 4.17). Some smaller specimens (Fig. 4.13–4.15) exhibit coarser, more subdued, irregular surfaces.


Lower Cambrian, Wernecke Mountains, Yukon Territory, Canada.


Qian and Bengtson (1989) synonymized several species within Archaeooides granulatus and a wide species concept has been applied to this genus. Specimens resembling Archaeooides in bearing a regular pustulose surface were assigned to Aetholicopalla adnata Conway Morris in Bengtson et al., 1990 (full synonymy by Demidenko in Gravestock et al., 2001). These genera seem to be distinct with the latter bearing a double-walled sphere with a central cavity filled with tubules, reticulation of the inner wall, and flattened surfaces of the sphere related to an encrusting habit (full synonymy by Demidenko in Gravestock et al., 2001). Some forms of Aetholicopalla Conway Morris in Bengtson et al., 1990 superficially resemble Archaeooides, but are distinguished by flattened surfaces and tubular pillars that connect the walls of the sphere. Aetholicopalla resembles Archaeooides when the external wall is not preserved (Wrona, 2004). Aetholicopalla is known from Australia (Conway Morris in Bengtson et al., 1990) and Germany (Elicki, 1998), and likely includes specimens previously assigned to Archaeooides such as those illustrated by Kerber (1988).

There is a wide variety of surficial features among specimens assigned to Archaeooides and among the material illustrated here. The largest difference is in the size and regularity of protuberances. A large specimen with many protuberances (Fig. 4.16) has a ratio of sphere diameter to protuberance diameter of 30:1 whereas smaller specimens (Fig. 4.14, 4.15) have a ratio of 8:1 (Table 1). Central openings of the protuberances represent either pores or broken spine bases (e.g., Yin et al., 2004). Interpretation as animal eggs may be supported by these protuberances that resemble those on modern invertebrate eggs (van Waveren, 1993). Although internal bodies were not observed within ornamented specimens which would better substantiate their interpretation as eggs, spheres do bear deflated surfaces similar to those on smooth egg envelopes, indicating that the membrane was originally flexible. The polar “X” shape (Fig. 4.17) is suggestive of cellular structure and may represent a four-celled embryo. More irregularly nodose surfaces of smaller specimens (Fig. 4.13–4.15) possibly represent multi-celled embryos with blastomeres exhibiting a “ghost” impression on the enclosing envelope, and although they resemble spawned invertebrate eggs (Young et al., 2002), embryonic developmental stages nor internal details were evident.

Forms included in Archaeooides may represent a variety of biological origins and we therefore refer the Wernecke material under open nomenclature, as Archaeooides sp. Morphological variation exhibited among the forms illustrated here demonstrates the need to have additional internal features such as described for Aetholicopalla to begin differentiating morphotypes. Some forms referred to Archaeooides may appear to preserve excystment (e.g., Chen, 1984), although these specimens may better be classified as Olivooides as they do not have tubercular ornaments. Forms such as Bacatisphaera Zhou, Brasier, and Xue, 2001 from the Duoshantuo Formation are spheroids with a pustulose surface sculpture that varies from loose to regular arrangement. These were interpreted as acritarchs.

Indeterminate spheroids Figure 5


A number of spherical fossils have morphological features that are different from those of Olivooides and Archaeooides. Two specimens are 425 μm in diameter with a finely porous envelope (Fig. 5.1–5.3) and are similar to porous spheroids from the Lower Cambrian of China were called Blastospongia polytreta Conway Morris and Chen, 1990. Pores are 10–15 μm wide (Fig. 5.1) and as small as 3 μm wide, possibly with fine spines preserved in the pores (Fig. 5.3). Some mushroom-shaped specimens were recovered that have smooth surfaces (Fig. 5.4). These globular specimens have one side that is broadly convex, a maximum diameter of 620 μm forming the “cap” of the mushroom, and one narrower (380 μm), flattened side forming the “stem” of the mushroom. One globular fossil (Fig. 5.5, 5.6) has triradial symmetry in which three equal-sized lobes are each 214 μm across and separated by broad sulci. The spheroid is as high as its maximum width. It is possible that this is an internal mold of Anabarites, but the preservation is unlike corroded molds that are dull in luster. A variety of elliptical spheroids were recovered, ranging in size from 540 μm long (Fig. 5.7) to 1.195 mm long (Fig. 5.8). Some forms are smooth and rounded at both ends (Fig. 5.7), while one has an open-ended stalklike structure, 100 μm long, at one end (Fig. 5.8). Similar ovate forms have been illustrated as Nephrooides speciosus Qian, 1977 (pl. 2, fig. 27) and ?Archaeooides by Ding and Qian (1988, pl. 4, fig. 14) and invite comparison with invertebrate eggs.

Anabaritids and Protoconodonts

Genus Anabarites Missarzhevsky, 1969

Type species

Anabarites trisulcatus Missarzhevsky, 1969.


Worldwide distribution summarized by Conway Morris and Chen (1989) and Missarzhevsky (1989).

Anabarites trisulcatus Missarzhevsky, 1969 Figure 6.1–6.4

Material examined

GSC 124010–124012, 123013.


Anabarites trisulcatus is the most abundant component of the fauna as noted by Nowlan et al. (1985). Many forms are similar to the type material, but wide preservational variation exists. Fragments are less than 1 mm long to almost 4 mm long, and range from less than 100 μm to more than 800 μm in width. Ends are either open or infilled with phosphate and no structure is preserved at either end. Shapes vary between straight, tapered, sinuous, and curved. Cross sections vary among specimens from circular to triradial (Fig. 6.1–6.3). Specimens with thin outer layers bear regularly spaced annulations perpendicular to the long axis (Fig. 6.4), but more commonly, the internal molds are preserved. Details of anabaritid wall structure described by Kouchinsky and Bengtson (2002) suggested an original aragonitic composition of the tube and possibly serpulid affinities.

Genus Protohertzina Missarzhevsky, 1973

Type species

Protohertzina anabarica Missarzhevsky, 1973.


China (Qian and Bengtson, 1989 and references therein), Siberian Platform and Kazakhstan (Missarzhevsky, 1973), India (Brasier and Singh, 1987), Australia (Bengtson et al., 1990), and North America (Conway Morris and Fritz, 1980; Nowlan et al., 1985; McIlroy and Szaniawski, 2000).


Protohertzina represents a genus that is in need of revision. Several species have been erected and distinguished using their cross sections (Missarzhevsky, 1977, fig. 1) and dimensions of the cone (curvature, length, width). Qian and Bengtson (1989) included several species of both slender and robust forms in the synonymy list of P. anabarica. Different species may represent different morphotypes of the same apparatus (Nowlan et al., 1985) in which variation of elements is suggested to form a P. anabaricaunguliformis plexus (Brasier and Singh, 1987). Although the task of revising Protohertzina is not addressed here, the present collection contains several morphotypes. As with the spherical fossils and Anabarites, preservation by phosphatization plays a role in systematics. Protohertzina specimens are long, delicate structures that are easily broken and many illustrated specimens in the literature do not show the nature of the base.

Protohertzina anabarica Missarzhevsky, 1973 Figure 6.5–6.8

Material examined

GSC 124014–124017.


Among the present collection, there are both compressed (anabariform) elements (Fig. 6.5) and more rounded (unguliform) elements (Fig. 6.6, 6.7). Phosphatic coatings of some specimens give them a smooth exterior, yet broken specimens reveal a fibrous cone internally (Fig. 6.7). Large forms (Fig. 6.8) with rounded bases comparable to P. robusta Qian, 1977 (synonymized with P. anabarica by Qian and Bengtson, 1989) are rare among the present collection and may represent a different species.

Protohertzina siciformis Missarzhevsky, 1973 Figure 6.9–6.14

  • Protohertzina siciformis Missarzhevsky, 1973, p. 56, text-fig. 6, pl. 9, fig. 5; 1977, fig. 1.8; Azmi and pancholi, 1983, pl. 1, fig. 8; Azmi, 1983, pl. 5, figs. 5–7, 9; Bhatt, Mamgain, and Misra, 1985, pl. 1, fig. 14; Ding and Qian, 1988, pl. 1, fig. 6.

  • ?Protohertzina cf. siciformis Missarzhevsky. Qian and Bengtson, 1989, p. 71–72, fig. 43; Bengtson, Conway Morris, Cooper, Jell, and Runnegar, 1990, p. 330–331, fig. 209.

  • Protohertzina anabarica Missarzhevsky. Brasier and Singh, 1987, “siciform” element, fig. 5.19, 5.20, 5.30.

  • Description

    Elements small (0.7–0.9 mm long), gently tapered, with long slender cusp, compressed posterior or posterolateral margin that forms keel at posterobasal corner and extends as long carina to cusp tip. Lateral ridges weak. Basal cavity deep. Base small with rounded to teardrop-shaped outline depending on development of carina. Laterally compressed element has rounded anterior margin, strong posterobasal keel and sharp posterior margin or carina, and weak lateral ridges (Fig. 6.9). More rounded elements have round basal outline and variable development of posterior carina (Fig. 6.10–6.14). Two fused clusters each containing two elements show variation in symmetry based on position of carina (Fig. 6.11, 6.12).

    Material examined

    GSC 124018–124023.


    Specimens are assigned to Protohertzina siciformis based on the most compressed element (Fig. 6.9) that resembles the type material in having a strongly compressed posterior edge and teardrop-shaped basal outline. Elements figured by Qian and Bengtson (1989) and Bengtson et al. (1990) resemble each other, but are questionably included in the present synonymy due to the shape of their bases, which are expanded and form an angle with the cusp. Brasier and Singh (1987) placed P. siciformis in synonymy with P. anabarica and described elements as “siciform,” but based on the present collection, two species are differentiated. The discovery of fused clusters herein assigned to P. siciformis suggests a complex protoconodont apparatus (Fig. 6.9– 6.14). Other reports of natural assemblages of protoconodonts include an “unassigned conodont cluster” from Iran (Hamdi, 1989), a pyritized cluster from Newfoundland described as Protohertzina? canadia McIlroy and Szaniawski, 2000, and clusters of P. robusta Qian, 1977 (Azmi and Paul, 2004). The apparatus described below invites comparison to the apparatus of the Late Cambrian protoconodont Phakelodus Miller, 1984 which has been compared to the grasping apparatus of recent chaetognaths (Szaniawski, 1982, 2002).

    Rodlike Fossils

    Genus Zhejiangorhabdion Yue and Zhao, 1993

    Type species

    Zhejiangorhabdion comptum Yue and Zhao, 1993.

    Original diagnosis

    “Small, slender, solid, straight, cylindrical or slightly tapering with round cross-section, phosphatic, rod-like fossils less than 1 mm long. Outer surface ornamented with nodes, spines, or cavities” (Yue and Zhao, 1993, p. 95).

    Zhejiangorhabdion comptum Yue and Zhao, 1993 Figure 7.1–7.17

  • Zhejiangorhabdion comptum Yue and Zhao, 1993, p. 98, pl. 1, figs. 1–7.

  • Description

    Cylindrical and tapering rodlike fossil with regular pattern of spherical depressions or hollows flanked by spiny projections along length of rod. Hollows packed along length of rod forming pattern like a honeycomb or egg carton. Flanking projections range from subdued nodes to well-developed, flattened, slightly tapering square-tipped spines. Rods range in length from greater than 2 mm (Fig. 7.1) to fragments 0.7 mm and shorter. Rods taper from wider, basal end to more slender, apical end. Range in width from 100 μm basally to 65 μm apically (slender form, Fig. 7.1), to more robust forms that taper subtly from 170 μm to 125 μm (Fig. 7.2). Some rods have well-preserved spines (Fig. 7.3–7.6) that have a maximum length of about 60 μm. Ends appear broken, but one specimen tapers to an almost hexagonal apical termination 80 μm across (Fig. 7.5). In lateral view, spines are rectangular with squared ends (Fig. 7.5). In plane view of tapered end of one specimen (Fig. 7.6, 7.7), they are more rounded nodes (possibly weathered), that arise from six points of a hexagon framing a hollow. Two spines of each segment of hexagon are shared by neighboring hollow (Fig. 7.7). On less-tapered, basal end of this specimen (Fig. 7.6, 7.8), spines are rectangular. Hollows are fairly regular along a rod, and range in size from 35 μm to 110 μm among various sizes of rods. Hollow spheres found preserved in hollows of some specimens (Fig. 7.6, 7.11).

    Hollow spheres that fill hollows range in size from about 30 μm across on a smaller rod (Fig. 7.11) to about 100 μm across on a larger rod (Fig. 7.8–7.10). On the larger rod, only one sphere is preserved. It is hollow, with outer layer or envelope and two concave discs on either side that may be envelopes of neighboring spheres. On the smaller rod, many spheres fill hollows (Fig. 7.11) and fewer spines are present. Spheres contact one another and are hollow, with outer envelope preserved between some spheres (Fig. 7.12, arrow). Small discs adhere to some spheres, with their concave sides facing adjoining hollow (Fig. 7.13–7.15). Discs are about 25 μm in diameter, some with a concave center that may open into sphere (compare to discs of Fig. 7.8, 7.10), and have thickened, rounded edges that are segmented along periphery (Fig. 7.14, 7.15, arrows). Smaller discs (14 μm in diameter) lie on some smaller spheres (Fig. 7.16, arrow).

    Material examined

    GSC 124024–124033.


    Lower Cambrian, East China, North America (this study).


    Material from the present study (more than 100 specimens) shows more variation in features than those described in the original diagnosis. The main difference in the ornament is due to preservation, whereby the Chinese material may have been more eroded to give the spines a nodose appearance. Yue and Zhao (1993) speculated on the affinities of this peculiar microfossil, comparing it to sponge and echinoid spines. The nature of the hollows and features of the spheres that fill them suggests the spheres can be biologically shed from the spiny rod and may represent some sort of reproductive structures. Discs that lie upon and between spheres vary in size with the smaller ones bearing segmentation. Some larger discs could possibly form the outer envelope between neighboring spheres. It is difficult to tell if the center of the small discs bears a hole, which may be infilled, or if the hollow center is due to erosion of the disc.

    Pyramidal, Conical, and Bulbous Fossils Figures 7.21, 8.1–8.3


    A pyramidal fossil (Fig. 7.21) is deeply hollow with a tapering shell that may curve slightly apically. Basal outline is broadly triangular, with a wide flat side, narrow flat side, and a gently outwardly convex side. A rounded keel forms the apex of the triangular base. Maximum width of base is 444 μm, tapering to apex that is 84 μm wide. Outline of the apex is oval. Walls are thin and outer surface lacks ornament. The specimen is somewhat similar to Tianzhusania described by Qian et al. (1979, pl. 2, figs. 17, 18, 25) but the cross section is not irregularly pentagonal, nor is there any longitudinal and transverse ornament.

    Two types of ornamented conical fossils were recovered that resemble Paradoxiconus typicalis Qian et al., 2001. One has a smooth conical apex and broad, tall, ornamented base that occupies two-thirds of the total height of the cone (1.13 mm) (Fig. 8.1). The apex is slightly concave on one (inner) side and convex (outer, figured side in Fig. 8.1) on the other. The tip of the apex is rounded and its cross section is oval. The entire base is ornamented by longitudinal, rounded ribs separated by grooves. The ornament is less pronounced about halfway along the cone and ribs are crenulated near the base of the cone. Many ribs have a bifurcating branching pattern. The base is buckled in a similar way to spheres and tubes within the biota (convex side, Fig. 8.1). Cone is infilled but the base was likely deeply hollow. A second form (Fig. 8.2) also has an oval cross section apically but is broken to reveal an infilled base. The base similarly has longitudinal ribs separated by grooves, but is broader. Where the cone is broken, this rib ornamentation gives a convolute oval outline. The ribs are ornamented by small nodes and some also exhibit a branched pattern (Fig. 8.2). The second form is closest to Type III of Paradoxiconus typicalis illustrated by Qian et al. (2001, pl. 1, fig. 8). These conical fossils may also be compared in outline to Acanthocassis He and Xie (1989), but the latter bears more prominent spines but less prominent “longitudinal radial lines” (He and Xie, 1989, plate 3, figs. 1–9). In addition, Steiner et al. (2004b) show that complete specimens of Acanthocassis have multiple spine-bearing arms and a subtending stem, which is very different from Paradoxiconus typicalis.

    One shelly fossil (Fig. 8.3) with a bulbous, netlike “base” (650 μm long) and slightly curved, ovate “stem” (500 μm long) was recovered. It appears broken at the bulbous end, which has a regular pattern of an open lattice with longitudinal and transverse ribs enclosing subquadrate depressions.

    Carinachitids Figure 8.4, 8.5


    One tetraradially symmetrical tube (Fig. 8.4–8.5), 370 μm high, with four broad, transversely ribbed faces separated by longitudinal furrows is assigned to Carinachites Qian, 1977, based on the emended diagnosis for the genus by Conway Morris and Chen (1992). The nature of the subdued ornamentation suggests some affinity to C. tetrasulcatus (Jiang in Luo et al., 1982), but the degree of tapering is much stronger in the latter species. Compaction flattened and imparted slight asymmetry to the fossil. Ridges on the faces have rounded crests.

    Tubes and Plates Figures 7.18–7.20, 8.6–8.19


    Phosphatized tubes and plates are abundant components in the present collection and are among the largest fragments, together with Anabarites (millimeter scale). Nowlan et al. (1985) described several of these fossils, but some additional forms are described briefly here to summarize the range of morphology within the biota. Several forms of hollow tubes occur. A hollow cylinder, 560 μm in diameter with walls 100–140 μm thick lacks any internal or external features and may be a coating of a tubular microfossil (Fig. 7.18). Another hollow cylindrical tube (Fig. 7.19) with one closed and one open end is 620 μm long and 322 μm across. It has thin walls, about 10 μm across, and lacks internal and external structure. Other similar-sized and shaped tubes that show tapering (Fig. 7.20) and are probably internal molds.

    Annulated rods are represented by the genera Hyolithellus Missarzhevsky, 1969, cf. Pseudorthotheca Cobbold, 1935, and ?Rugatotheca Cobbold and Pocock, 1934. Species of the genus Hyolithellus are distinguished by the nature and spacing of their transverse ribs. Specimens from the present collection are closest to Hyolithellus cf. H. isiticus Missarzhevsky, 1969 as illustrated by Nowlan et al. (1985, fig. 7) and similar to forms illustrated by Brasier and Singh (1987, fig. 8.3–8.5). Buckled and crumpled forms (Fig. 8.6, 8.7) show that the tubes distorted without fracturing, which may suggest they were flexible. Fragments range in length from a few millimeters to less than 0.5 mm. A similar form of annulated tube comparable to Pseudorthotheca has a small hole (Fig. 8.8, 8.9). Nowlan et al. (1985, fig. 10) also noted these borings that are similar to predatorial borings illustrated in Cambrian tubular fossils by Conway Morris and Bengtson (1994). Another form of annulated tube is also crumpled, and ornamented with transverse ribs separated by wrinkled longitudinal striae (Fig. 8.10). This tube is comparable to Rugatotheca but has broader spacing of ribs and better-developed striae than in forms illustrated by Yue and He (1989). It is also comparable to postembryonic stages of Olivooides referred to as the Punctatus/Pyrgites– type body fossils illustrated by Yue and Bengtson (1999, fig. 2), although no apical portions nor stellate surface sculpture were observed among the present collection.

    A wide variety of tuberculate and reticulate plates occur as millimeter-scale fragments (Fig. 8.11–8.19). These represent a range of forms bearing regularly distributed, subequal, rounded, moundlike tubercles (Fig. 8.11–8.13) and more defined, raised, and projecting tubercles (Fig. 8.14, 8.15). Of these forms, many are planar fragments, but some have a rounded shape, with tubercles covering all surfaces. The most complete example (Fig. 8.13) is ovate, with one closed, rounded end and one open end with a rounded outline. One plate has a reticulate structure with parallel, meandroid ribs alternating with rows of small depressions, 25 μm wide. The pattern becomes less defined toward one end of the plate (Fig. 8.16). A variety of large fragments have less distinct tubercles. One specimen has irregularly arranged, poorly defined, subspherical tubercles, up to 110 μm across, some of which have a centrally located slit (Fig. 8.17). A second form (Fig. 8.18) similarly has poorly defined tubercles (80 μm across) and a wrinkled surface upon which tubercles seem to lie in rows but may have been disturbed by crumpling of the specimen. A third form (Fig. 8.19) has a more regular ornament of small, indistinct tubercles, 50 μm across, and is irregularly incised by grooves.

    global comparisons and implications

    Initial reports of terminal Neoproterozoic and earliest Cambrian fossils were geographically scattered, triggering explanations for their distributions that focused on biogeography (McMenamin, 1982; Donovan, 1987). Fossil discoveries in western North America, such as Ediacaran dickinsoniids (Narbonne, 1994) and swartpuntiids (Hagadorn and Waggoner, 2000), calcified Neoproterozoic metazoans including Cloudina Germs, 1972 and Namacalathus Grotzinger, Watters, and Knoll, 2000 (Hofmann and Mountjoy, 2001), small shelly fossils from northwestern Canada (Conway Morris and Fritz, 1980; Nowlan et al., 1985), and now earliest Cambrian phosphatized eggs and microfossils (this report), are clarifying the originally cosmopolitan nature of these biotas. Cambrian paleogeographic configurations, although varied, suggest that Siberia and Laurentia may have remained in close proximity in an equatorial position until the Cambrian (Pelechaty, 1996; Sears and Price, 2000), while the South China Block was possibly part of East Gondwana in low latitudes during the Cambrian (Huang et al., 2000). The presence of strikingly similar animal eggs and embryos in similar Early Cambrian facies on three disparate continents emphasizes that these organisms were widespread biogeographically. Paleoceanographic conditions, perhaps linked to the carbonate ramp/platformal settings and associated climate of these three longitudinally separated regions, favored rapid phosphogenesis that preserved embryonic fossils.

    Reports of animal embryos augment the hidden or “missing” record of early animal evolution and some studies permit detailed embryonic reconstruction (e.g., Dong et al., 2004). Exceptionally preserved microfossils in North America reported here further fill an apparent gap in the seemingly stepwise fossil record of early animal evolution from the Neoproterozoic to the Cambrian, and emphasize the role of local environment and taphonomy in preserving these important microscopic remains. Taphonomic processes associated with rapid mineralization of metazoan eggs is becoming better understood through experimental work (Briggs and Wilby, 1996; Martin et al., 2003). Early Cambrian phosphorites and phosphatic limestones were widespread and volumetrically significant (Cook and Shergold, 1984), and reflect rapid phosphatization over large areas. As with the eggs and embryos described in this paper, many small shelly fossil assemblages were preserved through secondary phosphatization, and these are also widespread in Lower Cambrian strata, declining at the end of the Botomian Stage of the Early Cambrian synchronous with a decrease in the abundance of phosphatized facies (Porter, 2004).

    Brasier and Lindsay (2001) suggested explosive phases of evolutionary diversity are illusory, related to special preservational conditions controlled by the sedimentary record. It is through these phosphatization taphonomic windows that we are able to glimpse the record of an unexpectedly widespread biota, including the early record of animals with no calcified hard parts that would otherwise be destroyed by taphonomic processes or simply not preserved if the ocean chemistry was not suitable. The occurrence of phosphatized eggs and embryos in the Early Cambrian of North America is an example of exceptional mineralization associated with a phosphatization event. It is likely that investigation of similar environmental and taphonomic windows containing these “rare” assemblages will lead to additional significant discoveries in North America and elsewhere.


    This work was funded by Natural Sciences and Engineering Research Council operating grants to GMN and NPJ. Samples were processed by K. Paull, Geological Survey of Canada, Calgary. We thank D.-C. Lee for SEM imaging, C. Barnes for use of laboratory facilities, and S. Zhang for translation of Chinese literature. Reviews by M. Brasier, S. Bengtson, S. Conway Morris, and R. McNaughton improved the manuscript.



    F. J. Ayala, A. Rhetsky, and F. J. Ayala . 1998. Origin of the metazoan phyla: Molecular clocks confirm paleontological estimates. Proceedings of the National Academy of Sciences of the United States of America 95:606–611. Google Scholar


    R. J. Azmi 1983. Microfauna and age of the Lower Tal Phosphorite of Mussoorie Syncline, Garwhal Lesser Himalaya, India. Himalayan Geology 11:373–409. Google Scholar


    R. J. Azmi and V. P. Pancholi . 1983. Early Cambrian (Tommotian) conodonts and other shelly microfauna from the Upper Krol of Mussoorie Syncline, Garwhal Lesser Himalaya, with remarks on the Precambrian-Cambrian boundary. Himalayan Geology 11:360–372. Google Scholar


    R. J. Azmi and S. K. Paul . 2004. Discovery of Precambrian Cambrian boundary protoconodonts from the Gangolihat Dolomite of Inner Kumaun Lesser Himalaya: Implication on age and correlation. Current Science 86:1653–1660. Google Scholar


    J. Bahde, C. Baretta, L. Cederstrand, M. Flaugher, R. Heller, M. Irwin, C. Swartz, S. Traub, J. D. Cooper, and C. Fedo . 1997. Neoproterozoic–Lower Cambrian sequence stratigraphy, eastern Mojave desert, California: Implications for base of the Sauk sequence, craton-margin hinge zone, and evolution of the Cordilleran continental margin, p. 1–20. In G. H. Girty, R. E. Hanson, and J. D. Cooper (eds.), Geology of the Western Cordillera: Perspectives from Undergraduate Research. Pacific Section SEPM, Fullerton, California. Google Scholar


    S. Bengtson and Z. Yue . 1997. Fossilized metazoan embryos from the earliest Cambrian. Science 277:1645–1646. Google Scholar


    S. Bengtson, S. Conway Morris, B. J. Cooper, P. A. Jell, and B. N. Runnegar . 1990. Early Cambrian fossils from South Australia. Association of Australasian Palaeontologists Memoir, 9, 364 p. Google Scholar


    D. K. Bhatt, V. D. Mamgain, and R. S. Misra . 1985. Small shelly fossils of early Cambrian (Tommotian) age from Chert-Phosphorite Member, Tal Formation, Mussoorie Syncline, Lesser Himalaya, India and their chronostratigraphic evaluation. Journal of the Palaeontological Society of India 30:92–102. Google Scholar


    M. D. Brasier 1990. Phosphogenic events and skeletal preservation across the Precambrian Cambrian boundary interval, p. 289–303. In A. J. G. Notholt and I. Jarvis (eds.), Phosphorite Research and Development. Geological Society of London Special Publication, No. 52. Google Scholar


    M. D. Brasier and J. F. Lindsay . 2001. Did supercontinent amalgamation trigger the “Cambrian Explosion”?, p. 69–89. In A. Y. Zhuravlev and R. Riding (eds.), The Ecology of the Cambrian Radiation. Columbia University Press, New York. Google Scholar


    M. D. Brasier and P. Singh . 1987. Microfossils and Precambrian Cambrian boundary stratigraphy at Maldeota, Lesser Himalaya. Geological Magazine 124:323–345. Google Scholar


    D. E G. Briggs and P. R. Wilby . 1996. The role of calcium carbonate-calcium phosphate switch in the mineralization of soft-bodied fossils. Journal of the Geological Society, London 153:665–668. Google Scholar


    P. Chen 1984. Discovery of Lower Cambrian small shelly fossils from Jijiapo, Yichang, West Hubei and its significance. Professional Papers of Stratigraphy and Palaeontology 13:61–64. Google Scholar


    E. S. Cobbold 1935. Lower Cambrian faunas from Hérault, France. Annals and Magazine of Natural History (series 10) 16:25–48. Google Scholar


    E. S. Cobbold and R. W. Pocock . 1934. The Cambrian area of Rushton (Shropshire). Philosophical Transactions of the Royal Society of London, series B 223:305–409. Google Scholar


    S. Conway Morris and S. Bengtson . 1994. Cambrian predators: Possible evidence from boreholes. Journal of Paleontology 68:1–23. Google Scholar


    S. Conway Morris and M. Chen . 1989. Lower Cambrian anabaritids from South China. Geological Magazine 126:615–632. Google Scholar


    S. Conway Morris and M. Chen . 1990. Blastulospongia polytreta n. sp., an enigmatic organism from the Lower Cambrian of Hubei, China. Journal of Paleontology 64:26–30. Google Scholar


    S. Conway Morris and M. Chen . 1992. Carinachitiids, hexangulaconularids, and Punctatus: Problematic metazoans from the early Cambrian of South China. Journal of Paleontology 66:384–405. Google Scholar


    S. Conway Morris and W. H. Fritz . 1980. Shelly microfossils near the Precambrian Cambrian boundary, Mackenzie Mountains, northwestern Canada. Nature 286:381–384. Google Scholar


    P. J. Cook and J. H. Shergold . 1984. Phosphorus, phosphorites, and skeletal evolution at the Precambrian Cambrian boundary. Nature 308:231–236. Google Scholar


    P. T. Crimes and M. M. Anderson . 1985. Trace fossils from late Precambrian-Early Cambrian strata of southeastern Newfoundland (Canada); temporal and environmental implications. Journal of Paleontology 59:310–343. Google Scholar


    W. Ding and Y. Qian . 1988. Late Sinian to Early Cambrian small shelly fossils from Yangjiaping, Shimen, Hunan. Acta Micropalaeontologica Sinica 5:39–56. Google Scholar


    X-P. Dong, P. C J. Donoghue, H. Cheng, and J. Liu . 2004. Fossil embryos from the Middle and Late Cambrian Period of Hunan, South China. Nature 427:237–240. Google Scholar


    S. K. Donovan 1987. The fit of the continents in the late Precambrian. Nature 327:138–141. Google Scholar


    A. D'Orbigny 1842. Paléontologie Francaise. Text and Atlas. Masson, Paris, 662 p. Google Scholar


    J. Dzik 1994. Evolution of “small shelly fossils” assemblages of the Early Paleozoic. Acta Palaeontological Polonica 39:247–313. Google Scholar


    O. Elicki 1998. First report of Halkieria and enigmatic globular fossils from the Central European Marianian (Lower Cambrian, Gorlitz Syncline, Germany), p. 51–64. In V. Gamez, J. Antonio, T. Palacios et al. (eds.), Special Issue in Memory of Professor Gonzalo Vidal. Revista Espanola de Paleontologia, Special Issue. Google Scholar


    W. H. Fritz, G. M. Narbonne, and S. P. Gordey . 1983. Strata and trace fossils near the Precambrian Cambrian boundary, Mackenzie, Selwyn, and Wernecke Mountains, Yukon and Northwest territories. Current Research, Pt. B, Geological Survey of Canada Paper 83-1B:365–375. Google Scholar


    G. J B. Germs 1972. New shelly fossils from the Nama Group, South West Africa. American Journal of Science 272:752–761. Google Scholar


    D. I. Gravestock, E. M. Alexander, Y. E. Demidenko, N. V. Esakova, L. E. Holmer, J. B. Jago, T. Lin, L. M. Melnikova, P. Y. Parkhaev, A. Y. Rozanov, G. T. Ushantinskaya, and W. Zang . et al. 2001. The Cambrian Biostratigraphy of the Stansbury Basin, South Australia. Nauka/Interperiodica, Moscow, 343 p. Google Scholar


    J. P. Grotzinger, W. A. Watters, and A. H. Knoll . 2000. Calcified metazoans in thrombolitic stromatolite reefs of the terminal Proterozoic Nama Group, Namibia. Paleobiology 26:334–359. Google Scholar


    J. W. Hagadorn and B. Waggoner . 2000. Ediacaran fossils from the southwestern Great Basin, United States. Journal of Paleontology 74:349–359. Google Scholar


    B. Hamdi 1989. Stratigraphy and palaeontology of the Late Precambrian to Early Cambrian in the Alborz Mountains, northern Iran. Geological Survey of Iran Report 59:1–41. Google Scholar


    T. He and Y. Xie . 1989. Some problematic small shelly fossils from the Meishucunian of the Lower Cambrian in the western Yangtze region. Acta Micropalaeontologica Sinica 6:111–127. Google Scholar


    H. J. Hofmann and E. W. Mountjoy . 2001. NamacalathusCloudina assemblage in Neoproterozoic Miette Group (Byng Formation), British Columbia: Canada's oldest shelly fossils. Geology 29:1091–1094. Google Scholar


    B. Huang, R. Zhu, O. Yang, and Z. Yang . 2000. The Early Paleozoic paleogeography of the North China block and other major blocks of China. Chinese Science Bulletin 45:1057–1065. Google Scholar


    M. Kerber 1988. Mikrofossilien aus unterkambrishchen Gesteinen der Montagne Noire, Frankreich. Palaeontolographica A202:127–203. Google Scholar


    V. V. Khomentovsky and G. A. Karlova . 1993. Biostratigraphy of the Vendian–Cambrian beds and the Lower Cambrian boundary in Siberia. Geological Magazine 130:29–45. Google Scholar


    A. H. Knoll and S. B. Carroll . 1999. Early animal evolution: Emerging views from comparative biology and geology. Science 284:2129–2137. Google Scholar


    A. Kouchinsky and S. Bengtson . 2002. The tube wall of Cambrian anabaritids. Acta Palaeontologica Polonica 47:431–444. Google Scholar


    A. Kouchinsky, S. Bengtson, and L. Gershwin . 1999. Cnidarian-like embryos associated with the first shelly fossils in Siberia. Geology 27:609–612. Google Scholar


    G. Kumar, D. K. Bhatt, and B. K. Raina . 1987. Skeletal microfauna of Meishucunian and Qiongzhusian (Precambrian-Cambrian boundary) age from the Ganga Valley, Lesser Himalaya, India. Geological Magazine 124:167–171. Google Scholar


    G. Li and Y. Qian . 1999. A review of the research on the phosphatized spheroidal fossils in China. Acta Micropalaeontologica Sinica 16:287–296. Google Scholar


    T. S. Loutit, J. Hardenbol, P. R. Vail, and G. R. Baum . 1988. Condensed sections; the key to age determination and correlation of continental margin sequences, p. 183–213. In C. K. Wilgus, B. S. Hastings, C. A. Ross et al. (eds.), Sea-level changes; an integrated approach. SEPM Special Publication, 42. Google Scholar


    H. Luo, Z. Jiang, X. Wu, X. Song, and L. Ouyang . et al. 1982. The Sinian–Cambrian Boundary in Eastern Yunnan. People's Publishing House, Yunnan, 265 p. Google Scholar


    D. Martin, D. E G. Briggs, and R. J. Parkes . 2003. Experimental mineralization of invertebrate eggs and the preservation of Neoproterozoic embryos. Geology 31:39–42. Google Scholar


    D. McIlroy and H. Szaniawski . 2000. A lower Cambrian protoconodont apparatus from the Placentian of southeastern Newfoundland. Lethaia 33:95–102. Google Scholar


    M. A S. McMenamin 1982. A case for two late Proterozoic–earliest Cambrian faunal province loci. Geology 10:290–292. Google Scholar


    J. F. Miller 1984. Cambrian and earliest Ordovician conodont evolution, biofacies, and provincialism, p. 43–68. In D. L. Clark (ed.), Conodont Biofacies and Provincialism. Geological Society of America Special Paper, 196. Google Scholar


    V. V. Missarzhevsky 1969. Description of hyolithids, gastropods, hyolithelminths, camenids and forms of an obscure taxonomic position, p. 105–175. In A. Y. Rozanov et al. (eds.), The Tommotian Stage and the problem of the lower boundary of the Cambrian. Amerind Publishing, New Delhi, Trudy Akademiya Nauk SSSR. Google Scholar


    V. V. Missarzhevsky 1973. Conodont-shaped organisms from Precambrian-Cambrian boundary strata of the Siberian Platform and Kazakhstan, p. 53–57. In I. T. Zhuralev (ed.), Problemy paleontologii i biostratigrafii nizhnego kembriya Sibiri i Dal'nego vostoko. Trudy Instituta Geologii i Geofiziki SO AN SSSR, 49. Google Scholar


    V. V. Missarzhevsky 1977. Conodonts(?) and phosphatic problematica from the Cambrian of Mongolia and Siberia, p. 10–19, 91, 100, 106. In L. P. Tatarinov, B. Luvsandansan, Y. I. Voronin et al. (eds.), Bespozvonochnye Paleozoya Mongolii, Trudy-Sovmestnaya Sovetsko-Mongol'skaya Paleontologicheskaya Ekspeditsiya. Google Scholar


    V. V. Missarzhevsky 1989. The oldest skeletal fossils and stratigraphy of the Precambrian Cambrian boundary beds. Trudy Geologiceskogo Instituta AN SSSR 443:1–237. Google Scholar


    V. V. Missarzhevsky and A. J. Mambetov . 1981. Stratigraphy and fauna of Cambrian and Precambrian boundary beds of Maly Karatau. Trudy Akademii Nauka SSSR, Moscow, 326. Google Scholar


    J. F. Mount and D. Kidder . 1993. Combined flow origin of edgewise intraclast conglomerates; Sellick Hill Formation (Lower Cambrian) South Australia. Sedimentology 40:315–329. Google Scholar


    G. M. Narbonne 1994. New Ediacaran fossils from the Mackenzie Mountains, northwestern Canada. Journal of Paleontology 68:411–416. Google Scholar


    G. M. Narbonne and J. D. Aitken . 1995. Neoproterozoic of the Mackenzie Mountains, northwestern Canada. Precambrian Research 73:101–121. Google Scholar


    G. S. Nowlan, G. M. Narbonne, and W. H. Fritz . 1985. Small shelly fossils and trace fossils near the Precambrian Cambrian boundary in the Yukon Territory, Canada. Lethaia 18:233–256. Google Scholar


    D. T. Osborne, G. M. Narbonne, and J. Carrick . 1986. Stratigraphic and economic potential of Precambrian Cambrian boundary strata, Wernecke Mountains, east-central Yukon. Yukon Geology 1:131–138. Google Scholar


    S. M. Pelechaty 1996. Stratigraphic evidence for the Siberia-Laurentia connection and Early Cambrian rifting. Geology 24:719–722. Google Scholar


    S. M. Porter 2004. Closing the phosphatization window: Testing for the influence of taphonomic megabias on the pattern of small shelly fossil decline. Palaios 19:178–183. Google Scholar


    L. J. Pyle, G. M. Narbonne, N. P. James, R. W. Dalrymple, and A. J. Kaufman . 2004. Integrated Ediacaran chronostratigraphy, Wernecke Mountains, northwestern Canada. Precambrian Research 132:1–27. Google Scholar


    Y. Qian 1977. Hyolitha and some problematica from the Lower Cambrian Meishucunian Stage in central and southwestern China. Acta Palaeontologica Sinica 16:255–275. Google Scholar


    Y. Qian and S. Bengtson . 1989. Palaeontology and biostratigraphy of the Early Cambrian Meishucunian Stage in Yunnan Province, South China. Fossils and Strata 24:1–156. Google Scholar


    Y. Qian, M. Chen, and Y. Chen . 1979. Hyolithids and other small shelly fossils from the Lower Cambrian Huangshandong Formation in the eastern part of the Yangtze Gorge. Acta Palaeontologica Sinica 18:207–232. Google Scholar


    Y. Qian, G. Li, T. He, and Y. Xie . 2001. Helmet-like fossils from the basal Cambrian phosphoric strata of China. Acta Palaeontologica Sinica 40:486–496. Google Scholar


    J. W. Sears and R. A. Price . 2000. New look at the Siberian connection: No SWEAT. Geology 28:423–426. Google Scholar


    B. S. Sokolov and I. T. Zhuraleva . 1983. Lower Cambrian Stage Subdivision of Siberia, Atlas of Fossils. Trudy Instituta Geologii i Geofiziki SO AN SSSR 558, Moscow, 216 p. Google Scholar


    M. Steiner, M. Zhu, G. Li, Y. Qian, and B-D. Erdtmann . 2004a. New Early Cambrian bilaterian embryos and larvae from China. Geology 32:833–836. Google Scholar


    M. Steiner, G. Li, Y. Qian, and M. Zhu . 2004b. Lower Cambrian small shelly fossils of northern Sichuan and southern Shaanxi (China), and their biostratigraphic importance. Geobios 37:259–275. Google Scholar


    H. Szaniawski 1982. Chaetognath grasping spines recognized among Cambrian protoconodonts. Journal of Paleontology 56:806–810. Google Scholar


    H. Szaniawski 2002. New evidence for the protoconodont origin of chaetognaths. Acta Palaeontologica Polonica 47:405–419. Google Scholar


    J. W. Valentine 2002. Prelude to the Cambrian explosion. Annual Review of Earth and Planetary Sciences 30:285–306. Google Scholar


    A. K. Val'kov 1987. Lower Cambrian Biostratigraphy of the Eastern Siberian Platform. Nauka, Moscow, 137 p. Google Scholar


    I. M. van Waveren 1993. Morphology of Recent copepod egg envelopes from Turkey Point, Gulf of Mexico, and their implications for acritarch affinity, p. 111–124. In S. G. Molyneux and K. J. Dorning (eds.), Contributions to Acritarch and Chitinozoan Research. Special Papers in Paleontology, 48. Google Scholar


    Y. I. Voronin, L. G. Voronova, N. V. Grigorieva, N. A. Drosdova, E. A. Shegallo, A. Y. Zhuravlev, A. L. Ragozina, A. Y. Rozanov, T. A. Sayutina, V. A. Syssoiev, and V. D. Fonin . 1982. The Precambrian/Cambrian boundary in the Geosynclinal areas (The reference section of Salany-Gol, MPR). Transactions of the Joint Soviet-Mongolian Palaeontological Expedition, 18, Nauka Izdatelstvo, Moscow, 150 p. Google Scholar


    G. A. Wray, J. S. Levinton, and L. H. Shapiro . 1996. Molecular evidence for deep Precambrian divergences among metazoan phyla. Science 274:568–573. Google Scholar


    R. Wrona 2004. Cambrian microfossils from glacial erratics of King George Island, Antarctica. Acta Palaeontologica Polonica 49:13–56. Google Scholar


    S. Xiao and A. H. Knoll . 1999. Fossil preservation in the Neoproterozoic Duoshanto phosphorite Lagerstätte, South China. Lethaia 32:219–240. Google Scholar


    S. Xiao and A. H. Knoll . 2000. Phosphatized animal embryos from the Neoproterozoic Duoshantuo Formation at Weng'an, Guizhou, South China. Journal of Paleontology 74:767–788. Google Scholar


    S. Xiao, X. Yuan, and A. H. Knoll . 2000. Eumetazoan fossils in terminal Proterozoic phosphorites? Proceedings of the National Academy of Sciences, USA 97:13684–13689. Google Scholar


    S. Xiao, Y. Zhang, and A. H. Knoll . 1998. Three-dimensional preservation of algae and animal embryos in a Neoproterozoic phosphorite. Nature 391:553–558. Google Scholar


    Y. Xing, Q. Ding, H. Luo, T. He, and Y. Wang . 1984. The Sinian– Cambrian boundary of China and its related problems. Geological Magazine 121:155–170. Google Scholar


    C. Yin, S. Bengtson, and Z. Yue . 2004. Silicified and phosphatized Tianzhushania, spheroidal microfossils of possible animal origin from the Neoproterozoic of South China. Acta Palaeontologica Polonica 49:1–12. Google Scholar


    C. M. Young, M. A. Sewell, and M. E. Rice . 2002. Atlas of Marine Invertebrate Larvae. Academic Press, San Diego, 626 p. Google Scholar


    Z. Yue and S. Bengtson . 1999. Embryonic and post-embryonic development of the Early Cambrian cnidarian Olivooides. Lethaia 32:181–195. Google Scholar


    Z. Yue and T. He . 1989. A restudy of some Early Cambrian small shelly fossils from Ganluo and Emei, Sichuan, Southwest China. Acta Micropalaeontologica Sinica 6:389–407. Google Scholar


    Z. Yue and J-X. Zhao . 1993. Meischucunian (Early Cambrian) rod-like fossils from western Zhejiang. Acta Micropalaeontologica Sinica 10:89–97. Google Scholar


    X. Zhang and B. R. Pratt . 1994. Middle Cambrian arthropod embryos with blastomeres. Science 266:637–639. Google Scholar


    C. Zhou, M. D. Brasier, and Y. Xue . 2001. Three-dimensional phosphatic preservation of giant acritarchs from the terminal Proterozoic Duoshantuo Formation in Guizhou and Hubei provinces, South China. Palaeontology 44:1157–1178. Google Scholar

    Figure 1—Map of northwestern Canada showing generalized stratigraphy, location of phosphatized embryos in the Ingta Formation, and detail of the Ingta Formation.


    Figure 2—Scanning electron microscope (SEM) photomicrographs of fossil eggs and embryos referred to Olivooides sp. 1–4, Spheres with smooth outer membranes showing similar size of specimens and nature of indented and buckled surfaces, Sample 1680-1, GSC 123973, 123974, 123975, 123976; 5, large specimen showing collapse features and folding of membrane, Sample 1680-2, GSC No. 123977; 6, two-cell stage lacking smooth outer membrane, Sample 99127, GSC 123978; 7, 8, smaller spheres showing smooth membrane with polar indentation (on right side, 7) and two-cell stage lacking smooth outer membrane, 1680-2 and 1680-1/3, GSC 123979, 123980; 9, broken specimen showing thin egg envelope and possible blastomere boundary at arrows, Sample 1680-2, GSC 123981; 10, 11, broken specimen showing thin envelope at arrow in 10 (enlarged in 11), Sample 1680-2, GSC 123982; 12–14, hollow specimen filled with filaments that internally thicken the outer envelope, 13 shows spherulitic texture, 14 shows cross section and internal detail of diagenetically phosphatized filament, Sample 1680-1, GSC 123983; 15, hollow specimen showing thickening of outer envelope, internal filaments, and partially degraded inner body, Sample 99127, GSC 123984; 16–18, hollow specimen showing thickening of envelope (at arrows, detail in 17 and 18) by several layers of phosphate and internal coating of botryoidal phosphate, Sample 1680-2, GSC 123985.


    Figure 3—SEM photomicrographs of fossil eggs referred to Olivooides sp. 1, 2, Spheres with smooth outer membranes and centrally located sulcus, Sample 99127, GSC 123986, 123987; 3, 4, cross-sectional view of hollow specimen with sulcus showing infolding of envelope, arrow points to radial fibrous apatite crystals (detailed in 4) infilling interior of sphere, Sample 99127, GSC 123988.


    Figure 4—SEM photomicrographs of spheres referred to Archaeooides sp. 1, Spherical form, Sample 99139, GSC 123989; 2, deflated sphere, Sample 99127, GSC 123990; 3, 4, sphere with deflated surface and detail of protuberances, Sample 1680-2, GSC 123991; 5, highly deflated sphere showing preservation of protuberances in deflated surfaces, Sample 99127, GSC 123992; 6–8, deflated hollow sphere with detail of protuberances (7) and detail of thin wall (at arrow in 6) and internal filament with spherulitic texture (at arrow in 8), Sample 99139, GSC 123993; 9, 10, regularly ornamented spheres, Sample 1680-2, GSC 123994, 123995; 11, deeply deflated, ornamented sphere, Sample 99127, GSC 123996; 12–15, small spheres, Samples 1680-3, 1680-2, 1680-2, 1680-1/3; GSC 123997, 123998, 123999, 124000; 16, large sphere, Sample 1680-2, GSC 124001; 17, ornamented sphere with polar “X,” Sample 1680-3, GSC 124002; 18, coarsely ornamented sphere, Sample 1680-2, GSC 124003.


    Figure 5—SEM photomicrographs of indeterminate spheroids. 1–3, Porous spheres, with detail of pores bearing fine spines (at arrows in 3), Sample 1680-2, GSC 124004, 124005; 4, mushroom-shaped spheroid, Sample 1680-2, GSC 124006; 5, 6, triradiate spheroid, Sample 1680-2, GSC 124007; 7, 8, ovate spheroids, Samples 1680-1/3, 99143, GSC 124008, 124009.


    Figure 6—SEM photomicrographs of Anabarites trisulcatus Missarzhevsky, 1969, 1, 3, Sample 14A3, 2, Sample 99136, 4 Sample 1680-1/3, GSC 124010, 124011, 124012, 123013; 5-8, Protohertzina anabarica Missarzhevsky, 1973, all from Sample 99139, 5, anabariform element, GSC 124014, 6, 7, unguiliform elements, GSC 124015, 124016, 8, element comparable to P. robusta Qian, 1977, GSC 124017; 9–14, Protohertzina siciformis Missarzhevsky, 1973, symmetry transition of elements and fused clusters, Sample 1680-1/3, GSC 124018, 124019, 124020, 124021, 124022, 124023.


    Figure 7—SEM photomicrographs of Zhejiangorhabdion comptum Yue and Zhao, 1993 and other phosphatized fossils. 1–17, Z. comptum, all from Sample 1680-1/3. 1–3, Size range of rod, GSC 124024, 124025, 124026; 4, 5, spiny fragment and apical view, GSC 124027; 6–10, rod with sphere in hollow, GSC 124028, 7, detail of hollows in apical portion outlined in 6, 8–10, detailed views of basal portion outlined in 6; 11–17, rod with many spheres contained in hollows, GSC 124029; 12, enlarged view of basal end, arrow pointing to outer envelope, 13, enlarged view of right side with segmented discs at arrows, 14, 15, detail of discs, arrows pointing to marginal segmentation of discs, 16, enlarged view of distal portion, disc at arrow detailed in 17. 18–20, Hollow cylindrical tubes, 18, 19, Sample 1680-1/3, GSC 124030, 124031, 20, Sample 99143, GSC 124032; 21, hollow, pyramidal fossil, Sample 1680-1/3, GSC 124033.


    Figure 8—SEM photomicrographs of phosphatized fossils, carinachitids, tubes, and plates. 1, 2, Paradoxiconus typicalis Qian et al., 2001, Sample 1680-1/3, GSC 124034, 124035; 3, indeterminate bulbous fossil, Sample 99127, GSC 124038; 4, 5, Carinachites sp., Sample 1680-1/3, GSC 124037; 6, 7, Hyolithellus cf. H. isiticus Missarzhevsky, 1969, Sample 99127, GSC 124038, 124039; 8, 9, cf. Pseudorthotheca sp., detail of boring (at arrow in 9, detail in 8), Sample 1680-1/3, GSC 124040, 10, ?Rugatotheca sp., Sample 99127, GSC 124041; 11–19, ornamented plates, 11–13, Sample 14A3, GSC 124042, 124043, 123044; 14, 15, Sample 99139, GSC 124045, 124046; 16, Sample 14A3, GSC 124047; 17, 18, Sample 99139, GSC 124048, 124049, 19, Sample 1680-1/3, GSC 124050.


    Table 1—Ratio of maximum sphere diameter to protuberance diameter.

    Accepted: 1 June 2005; Published: 1 September 2006
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