Graptolite-like fibril pattern in the fusellar tissue of Palaeozoic rhabdopleurid pterobranchs
PIOTR MIERZEJEWSKI and CYPRIAN KULICKI
Mierzejewski, P. & Kulicki, C. 2001. Graptolite-like fibril pattern in the fusellar tissue of Palaeozoic rhabdopleurid pterobranchs. - Acta Palaeontologica Polonica 46, 3, 349-366.
The fusellar tissue of Palaeozoic rhabdopleurid pterobranchs has been studied using the SEM techniques. The fibrillar material of Ordovician Kystodendron ex gr. longicarpus and Rhabdopleurites primaevus exhibits a distinct dimorphism, comprising: (1) thinner, wavy and anastomosing/branching fusellar fibrils proper, producing a tight three-dimensional meshwork; and (2) long, more or less straight and unbranched cortical fibrils, sometimes beaded, and arranged in parallel. These fibrils are similar to the fusellar and cortical fibrils of graptolites, respectively. Until now, dimorphic fibrils and their arrangement within fusellar tissue were regarded as unique characters of the Graptolithina. In general, the fibrillar material of these fossils is partially preserved in the form of flaky material (new term) composed of flakes (new term). Flakes are interpreted as flattened structures originating from the fusion of several neighbouring tightly packed fibrils. A Permian rhabdopleurid, referred to as Diplohydra sp., reveals a fabric and pattern of fusellar tissue similar to that of both Ordovician rhabdopleurids but devoid (?) of cortical fibrils. The results presented here question views that: (1) substantial differences in fabric and pattern of fusellar tissue exist between fossil pterobranchs and graptolites; and (2) the ultrastructure of pterobranch periderm has remained unchanged at least since the Ordovician. The Palaeozoic rhabdopleurids investigated are closer ultrastructurally to graptolites than to contemporary pterobranchs. The pterobranchs and the graptolites should be treated as members of one class – the Graptolithoidea.
Key words: Pterobranchs, rhabdopleurids, graptolites, ultrastructure, periderm, taxonomy, Ordovician, Permian.
Piotr Mierzejewski [firstname.lastname@example.org], Instytut Paleobiologii PAN, ul. Twarda 51/55, PL-00-818 Warszawa, Poland. Present address: ul. Filtrowa 83 m. 49, PL-02-032 Warszawa, Poland.
Cyprian Kulicki [email@example.com], Instytut Paleobiologii PAN, ul. Twarda 51/55, PL-00-818 Warszawa, Poland.
Living and fossil pterobranchs of the order Rhabdopleurida have an organic sclerotized exoskeleton (also termed coenecium or tubarium) made of regular growth bands called fuselli or fusellar increments. Comparable growth bands, but more irregular in form and spacing, are known in the other pterobranch order, the Cephalodiscida. According to Koz³owski (1938, 1949, 1966), the fusellar tissues of the Pterobranchia and the Graptolithina are homologues. He was convinced “that a structure of such type does not occur in any other animal, either Recent or fossil” (Koz³owski 1966: p. 497). Nevertheless, several researchers questioned the homology of skeletal tissues in both groups (e.g. Bohlin 1950; Decker 1956; Hyman 1959; Kirk 1972, 1974, 1975; Urbanek 1976a, b ; for a detailed discussion of this question, see Urbanek 1986, 1987). In spite of the supposedly sharp differences between the fabric of fusellar tissue in both groups at the submicroscopic level (Urbanek 1976a, b, 1978, 1986, 1987), it is widely accepted that pterobranchs and graptolites are descended from a common ancestor and had formed independent phylogenetic lines as early as in Cambrian times (see, for example: Rickards 1975; Crowther 1981; Urbanek 1986; Chapman et al. 1996). However, it should be stressed that present knowledge of the fine structure of fossil and living pterobranchs’ skeletal tissues is still incomplete and based on a limited number of investigations (see below, p. 000).
Our SEM study examined the fine structure of the fusellar tissue of some Palaeozoic rhabdopleurids in order to verify Urbanek’s (1976a, b) claims that the characteristic ultrastructural fabric and pattern of rhabdopleurid skeletal tissue are invariable, have remained unchanged at least since the Ordovician, and are dissimilar to those of graptolites. His publications played a major role in the longstanding debate about the affinities of graptolites (for historical details of this discussion, see Urbanek 1986, 1987). Urbanek’s morphogenetic and phylogenetic theses were based on TEM studies of the fusellar tissue of both fossil and Recent Pterobranchia; he strongly questioned Koz³owski’s (1938, 1949, 1966) ideas concerning a pterobranch ancestry for graptolites but failed to win acceptance (e.g. Andres 1977, 1980; Crowther & Rickards 1977; Crowther 1978, 1981; Crowther in Urbanek 1978, p. 627). Nevertheless, his ultrastructural observations and his conclusions regarding the supposedly substantial and invariable differences between the fusellar components of graptolite and pterobranch skeleton (Urbanek 1976a, b) have been widely adopted and gone largely unchallenged for a quarter of a century.
The Ordovician and Permian material selected for the present study represents different rhabdopleurid families. The Ordovician Kystodendron ex gr. longicarpus (Eisenack) and Rhabdopleurites primaevus Koz³owski are members of the Rhabdopleuridae and the Rhabdopleuritidae, respectively (for taxonomy of the Rhabdopleurida see Mierzejewski 1986). Both examples were derived from Gilbergabrottet 1, a well-known exposure of the Ontikan Limestones of Valaste age (lower Llanvirn) deposits in northernmost Öland, Sweden (for details of location, lithology, fauna and biostratigraphy, see Bohlin 1949 and Grahn 1980). Using 10-15 % acetic acid the material was etched out of a sample of grey glauconitic limestone (ca. 0.5 kg), collected by the first writer (together with Dr S. Stouge) in 1985 during his stay at the Institute of Historical Geology and Palaeontology, University of Copenhagen. The incertae familiae Permian rhabdopleurid referred to as Diplohydra sp. comes from the core Dia 84-31 (sample P3, depth 10.18.-10.40 m.), Svalis Dome, central Barents Sea, Norway; it was obtained from an undescribed microfossil collection made by A. Mørk, H.A. Nakrem and H. Szaniawski. The age of this material has been estimated as Kazanian on the basis of palynomorphs (Nilsson et al. 1996); an associated rich assemblage of scolecodonts is discussed by Nakrem et al. (in press). The specimen was etched from a cherty mudstone matrix using acetic and hydrofluoric acid.
All specimens studied were coated with platinum and examined using a Philips SEM XL 20. Dimensional data quoted in the text were taken directly from the SEM. The rhabdopleurid material described has been deposited in the Institute of Palaeobiology, Polish Academy of Science, Warsaw (abbreviated ZPAL).
The standard terminology for graptolite periderm ultrastructure (defined by Urbanek & Towe 1974) is adhered to in this work. However, two new terms are introduced:
(i) flake – structure composed of several tightly packed fibrils lying approximately in the same plane and cemented together to form an irregular plate.
(ii) flaky material – material composed of flakes, usually intermingled with free-lying fibrils.
Previous EM studies of pterobranch skeletal tissues
TEM studies of rhabdopleurid pterobranch skeletal tissues began with work of Wetzel (1958). He compared the fine structure of the fusellar zooidal tube of Recent Rhabdopleura with the prosicular non-fusellar periderm of an Ordovician diplograptid, Orthograptus gracilis (Roemer). He found no resemblance but noted that both rhabdopleuracean and graptolite skeletal tissues are made predominantly of fibrous material. Rickards & Dumican (1984: p. 176) emphasized that Wetzel was also the first to discover “the contrast in dimensions between the fibrils in O. gracilis and Rhabdopleura, the latter being finer and, apparently, often straighter and needle-like even in thin sections”.
The frame of reference for all future ultrastructural studies of rhabdopleurid periderm was set by Dilly (1971) in his excellent study of Recent Rhabdopleura compacta (Hincks). According to Dilly, the fusellar tissue of this pterobranch is built of a mass of keratin-like straight fibrils, loosely dispersed in an almost structure-free matrix. The fibrils are of three different types when classified by their ultrastructural features and vary considerably in length, from a few nanometers to over 5 m m. The thickest fibrils have a diameter of about 25-30 nm and contain a double helix of fine fibrils. As demonstrated by Urbanek (1976a, b), the coenecium of the living cephalodiscid pterobranch Cephalodiscus (Cephalodiscus) inaequatus (Andersson) is ultrastructurally very similar to that of Recent Rhabdopleura. Unfortunately, the state of preservation of his material precluded any closer analysis of the Cephalodiscus fibrils. Later, Urbanek, Dilly & Mierzejewski (in Mierzejewski 1984b) found that the skeletal tissue of Recent Cephalodiscus solidus Andersson is built of straight, unbranched fibrils which possess a large lucent core. The diameter of these fibrils varies in the range 19-22 nm. Regretably, extensive SEM and TEM studies by P.N. Dilly, A. Urbanek and P. Mierzejewski made in 1981 on three living species of Cephalodiscus remain unpublished; only some of their observations and conclusions are mentioned by Mierzejewski (1984b), Urbanek (1986) and herein. Dilly’s (1993) SEM and TEM studies showed that spines of Recent Cephalodiscus graptoloides Dilly have an identical structure to a graptolite nema. Additional TEM and SEM observations were made by Andres (1980) and Crowther (1981) on the fine structure of Recent cephalodiscid and rhabdopleurid coenecial tissue, respectively.
Ultrastructural studies of fossil pterobranchs also have a short history and are restricted only to the TEM and SEM investigations of Urbanek (1976a, b), Andres (1980), Mierzejewski (1984a, 1986) and Urbanek et al. (1992); Rickards et al. (1984: p. 27) unsuccessfully applied SEM techniques to the periderm of Silurian Rhabdopleura hollandi. The observations and conclusions of Urbanek (1976a,b) are of special significance. He investigated the fusellar tissue of two fossil rhabdopleurids: the Ordovician Rhabdopleurites primaevus Koz³owski, 1967 and the Jurassic Rhabdopleura kozlowskii Kulicki, 1969. He concluded that the nature and arrangement of fusellar fibrils within the Pterobranchia are invariable and have remained unchanged since at least the Ordovician. He also concluded that the striking dissimilarity between fibrillar material of Pterobranchia and Graptolithina rules out any close affinity of between them. Previous TEM studies carried out by Towe & Urbanek (1972), Berry & Takagi (1973) and Urbanek & Towe (1974, 1975) demonstrated that the fusellar tissue of graptolites is composed of a different fibrillar fabric from that of Recent Rhabdopleura. Graptolite fusellar fibrils, presumably of a collagenous nature, are distinctly thicker and their average diameter varies usually in the range 60-110 nm (Crowther 1981), and reaches up to 130 nm (Bates 1997). Moreover, they are not straight and loosely dispersed but wavy, branching or anastomosing, creating a three-dimensional spongy meshwork.
In these circumstances, the discovery that the coenocia of Recent cephalodiscid and rhabdopleurid pterobranchs are collagenous (Armstrong et al. 1984) appeared to be of great importance. It reinforced the hypothesis that pterobranchs and graptolites are phylogenetically closely related and explained differences at the ultrastructural level as a secondary effect of the arrangement of tropocollagen units within the collagen fibrils. In connection with this discovery, Urbanek (1986, 1987) introduced the term “ultrastructural anomaly” for the ultrastructural differences between the fibrillar material of both groups, and he attached great significance to the distinction. He regarded such ultrastructural differences as “one of the best criteria for the pterobranch-graptolite boundary in phylogeny and classification” (Urbanek 1986: p. 211) and stated later that “Perhaps they are among the best diagnostic features of the graptolite grade of the rhabdosome construction” (Urbanek 1987: p. 228). It is the more remarkable then that the periderm of the Middle Cambrian Rhabdotubus johanssoni Bengtson and Urbanek (one of the two oldest known rhabdopleurids) reveals in some cases a delicate network of interconnected fibrils, indicating an essentialy graptolite grade of periderm fine structure (Urbanek et al. 1992: fig. 1).
Kystodendron ex gr. longicarpus (Eisenack)
Description. - The specimen examined is a small fragment of coenecium consisting of an upright zooidal tube joined to a piece of creeping tube (Fig. 1A). The fossil is preserved undistorted and in full relief. With regard to the state of preservation, it differs from all other chemically isolated Ordovician rhabdopleurids (described by Koz³owski 1967, 1970, and Mierzejewski 1986) in the considerable rigidity of its periderm and a strong pigmentation.
The preserved fragment of creeping tube is semicircular in transverse section, ca. 300 m m long and 90 m m wide, with a flat lower wall (the basal membrane) and a convex upper wall. The lower wall, which was attached to the substratum during the organism’s life, is light brown, semi-transparent and looks strongly crumpled; it shows no traces of fibrillar structure. The upper wall is dark brown, opaque and displays a distinctly fusellar structure. Fuselli occur on both sides of the upper wall and join each other at a constant angle to form a characteristic zigzag suture. The width of the fuselli varies considerably, between 10.5 m m and 13.1 m m. The creeping tube is bordered by a narrow, structureless marginal membrane, which is colourless and almost translucent (Fig. 1C).
The zooidal tube is 730 m m long, built of very clear fuselli and extends perpendicular to the creeping tube (Fig. 1A, B). It is almost cylindrical, robust, and mostly dark brown and opaque; the most distal section is lighter in colour. There is a distinct and rather gradual increase in width of the zooidal tube, from 61 m m at the base to 90 m m at the aperture. Fuselli of the zooidal tube are complete rings, with a single oblique suture - similar to those of most rhabdopleurids (Figs 1B, 2). The upper margins of the fuselli protrude strongly to produce a characteristic fusellar collar (Figs 1A,B, 2). The spacing of fusellar increment spacing is about 60 per mm; the height of the fuselli (i.e. the distance between the growth lines) ranges between 16.5 and 21.4 m m.
The fine structure of the surface of the fusellar periderm is very well preserved. The outer surface was primarily covered with a smooth, presumably homogenous, enamel-like pellicle (Fig. 2). Only in some places is the pellicle fractured; minor foldings and finely comminuted debris make original features less distinct. Most of the debris is probably composed of exfoliated fusellar pellicle (Fig. 3A). Usually the pellicle is robust and masks the inner fusellar structure, but in some places, it seems to be more delicate and reflects the shape and orientation of underlying fusellar fibrils (Fig. 3B). However, the fibrillar material becomes especially clear when the fusellar pellicle has been damaged and removed. Here the fusellar fibrils can be subdivided into two categories according to their shape and thickness: (1) short, wavy, branched or anastomosing fusellar fibrils proper; and (2) long and straight, distinctly thicker cortical fibrils. However, sometimes fibrils intergrade between these two types. Fibrils of the first category build the main fibrillar component of the fusellar tissue. They are usually ca. from 70 to 90 nm in diameter, sometimes reaching to 110 nm or more. Fusellar fibrils are usually more or less close-packed and produce a characteristic, three-dimensional, reticulate pattern (Figs 3B, 4). At some places the packing together of the fibrils appears distinctly loose (Fig. 4B). There are also intercalations of almost homogenous material which we term flakes (Fig. 4). In some cases, the flakes pass gradually into strongly packed and then loose-lying fibrils (Fig 4C). Fibrils of the second category occur exclusively in the collars of fuselli (Fig. 3). SEM micrographs distinctly show that each fusellar collar is built of closely packed or even cemented cortical fibrils. They are arranged uniformly and parallel to the margins of collars, forming a band-like, solid construction. Like the fibrils of the first category, the cortical fibrils are not uniform in thickness, with thinner fibrils being scattered among thicker ones; their diameter varies from 150 to 200 nm. Sometimes, extremely thick cortical fibrils occur, up to 290 nm in diameter, but presumably these result from the fusion of two or more thinner fibrils. When examined at higher magnification, neither fusellar fibrils proper nor cortical fibrils show show traces of substructure or annular ringing. There is no indication of a preserved ground substance in between the fibrils.
Remarks. - The morphology of this specimen of Kystodendron ex gr. longicarpus matches the zooidal and creeping tubes of living members of the genus Rhabdopleura Allman, 1869. Almost identical specimens, composed of erect and creeping tubes, were described from Ordovician erratic boulders by Koz³owski (1970) and Mierzejewski (1986), who referred them to Eorhabdopleura urbaneki Koz³owski (this specific name is treated as a nomen dubium, see Mierzejewski 1986, p. 184) and Kystodendron longicarpus (Eisenack), respectively. The first author of the present paper examined several similar specimens from the Ordovician of Estonia (found in the undescribed collection of the late Dr Ralph Männil) which, by rhabdopleurid standards, represent an exceptionally small sized pterobranch; it may be best compared with the smallest known forms of the fossil Rhabdopleuridae, i.e. Kystodendron tener Mierzejewski, 1986 and K. ex gr. longicarpus (Eisenack), known from Ordovician and Silurian glacial drift boulders (Mierzejewski 1986). As in Rhabdopleura (see Urbanek & Dilly 2000), the zooidal tubes of Kystodendron have only limited value in the identification of species, so the use of open nomenclature is necessary.
SEM studies of the ultrastructure of zooidal tubes of recent Rhabdopleura compacta Hincks, 1880 have revealed the presence of fibrils on the outer surface of fuselli (Dilly 1976). These fibrils are external to the main body of the periderm; long fibrils which cross several increment rings, and short fibrils which run along the height of each fusellus can be distinguished. The periderm of the specimen described here is entirely devoid of such external fibrils. It rather resembles the smooth, enamel-like external surface of the periderm of various sessile graptolites (see Urbanek et al. 1980).
The fine structure of the non-fusellar skeletal elements of the tubarium of Kystodendron (stolons and sterile bud cysts) was studied under the TEM by Mierzejewski (1986). The material comprising these elements appears to be completely homogenous.
Rhabdopleurites primaevus Koz³owski, 1967
Description. – The specimen studied (Fig. 5A) is a fragment of a strongly flattened zooidal tube measuring 760 m m in length and ca. 340 m m in width. It is composed of delicate, flexible, light-brown and translucent periderm. The fusellar increments are usually ring-like, only rarely exhibit an oblique suture and vary from 30 to 61 m m in width. The fusellar collars are weak and indistinct; some appear to be empty.
The periderm surface is patchy (as defined by Urbanek 1986, p.210) and rough (Fig. 5B). No distinct fibril network can be identified in the periderm material. The fusellar tissue is composed largely of strongly condensed flaky, material with rare meshes (Fig. 6). Most flakes appear to be structureless (to the limits of SEM resolution). In some, however, more or less wavy and free-laying fusellar fibrils pass into flakes, or flakes are clearly built of aggregations of tightly packed and cemented fibrils (Fig. 6). The diameter of these fibrils varies between wide limits, from as little as 90 nm up to 200 nm. Moreover, the straighter and thicker cortical fibrils (usually 200-240 nm in diameter) occur sporadically in fusellar collars (Fig. 6E). These fibrils possess annular thickenings with a rather irregular periodicity of about 150 nm.
Remarks.- The specimen agrees closely in shape and dimensions with those from Ordovician glacial boulders described by Koz³owski (1967, 1970) and Mierzejewski (1986), and studied ultrastructurally under the TEM by Urbanek (1976a, b). Previously Skevington (1965) erroneously described these forms from the Ordovician of Öland by as ?Graptovermid sp., gen. et sp. indet., as noted by Andres (1977) and Mierzejewski (1977, 1986). Contrary to Skevington’s specimens, ours is devoid of an inner secondary layer (first recognized in rhabdopleurid pterobranchs by Kulicki 1971).
The nature of certain characteristic “patches” on the periderm surface is unclear. They may result from corrosion of the primary surface prior to fossilization and represent the remnants of a fusellar pellicle fused with flaky material. On the other hand, they reveal a striking similarity to the “patches” which cover the surface of living tubes of some Recent cephalodiscid pterobranchs, as discovered by Dilly, Urbanek and Mierzejewski (unpublished), and subsequently interpreted as secondary deposits (cf. Urbanek 1986: p. 210).
The fine structure of the fusellar tissue of Rhabdopleurites primaevus is of crucial importance both for Urbanek’s (1976a, b) claim that substantial differences exist between pterobranch and graptolite fibrllar material and for the existence of his “ultrastructural anomaly”. His investigation, micrographs and conclusion are reinterpreted below and compared with the SEM studies reported here. The ultrastructure of the remaining elements of the coenecium was investigated by Mierzejewski (1986), who discovered that non-fusellar tubes are built of periderm showing a clearly laminar ultrastructure, whereas stolons are built of very thin, long and straight fibrils, cemented together.
Description. – The specimen studied represents a fragment of a rhabdopleurid coenecium; it is composed of several branching, tangled stolons connected to remnants of fusellar tubes. A detailed morphological description of this fossil is outside the scope of the present paper and will be published elsewhere (Mierzejewski & Kulicki, in preparation). Like the stolons, the fragments of the fusellar tubes are generally flattened, and their micromorphological details (e.g. sutures between fuselli or fusellar collars) are difficult to observe. However, the fine structure of the fusellar tissue is well seen under the SEM (Fig. 7A). The predominant component is flaky material together with some fibrils (diameter 100-150 nm), producing an irregular three-dimensional network. The characteristic meshes of this network are distributed randomly and attain a diameter of 0.7-1.1 m m. The gradual passage from free-lying fibrils into more or less condensed flakes is observed.
Sometimes, the fibrillar material is seen on the outer surface of the stolon, forming a layer of very tightly packed fibrils (Fig. 7B). These fibrils are randomly oriented and seem to be rather short and wavy; their diameter varies between 110 and 170 nm. Flaky material is not observed among these fibrils.
No trace of any long straight fibrils, similar to that of Kystodendron and Rhabdopleurites, are found in the fusellar tissue or on the outer surface of the stolon.
Remarks. – While the pattern of fusellar tissue in the fossil under discussion differs from that of living Rhabdopleura compacta (see Dilly 1971), it is very similar to that of Ordovician Kystodendron and Rhabdopleurites (herein), apart from the lack of long, thick, parallel packed cortical fibrils. On the other hand, the mass of fibrils covering the stolons of Diplohydra sp. is strikingly similar to a condensation of thick fibrils incorporated within the stolonal wall of Recent Rhabdopleura compacta (Hincks) (Dilly 1975, fig. 12), and of Ordovician Rhabdopleurites primaevus Koz³owski (Mierzejewski 1986, pl. 27:2).
It is noteworthy that Diplohydra sp. is the first pterobranch (and the first representative of the phylum Hemichordata) to be found in Permian deposits.
The results of this SEM study of Palaeozoic rhabdopleurid pterobranchs are in sharp contrast with those of Urbanek’s (1976a, b) TEM studies. Urbanek stated that the fabric of the fusellar tissue in pterobranchs differs essentially from that of graptolites, and that the nature and arrangement the fusellar fibrils within the Pterobranchia have not changed since the Ordovician.
In contrast, we have found no fundamental ultrastructural difference between the fusellar tissues of graptolites and Palaeozoic rhabdopleurid pterobranchs. The fusellar tissue of Ordovician Kystodendron ex gr. longicarpus (Eisenack) and Rhabdopleurites primaevus, as well as Permian Diplohydra sp., reveals a fabric made of fibrils strikingly similar to those recognized in graptolites. The fusellar fibrils of these forms are not thin and needle-like, as in Recent Rhabdopleura, but thick and wavy, as in graptolites. Moreover, the diameter of graptolite fusellar fibrils (60-110 nm according to Crowther, 1981; exceptionally up to 130 nm, see Bates, 1997) and that of Palaeozoic rhabdopleurids (70-150 nm, sporadically up to 200 nm, herein) is similar whereas fusellar fibrils in Recent Rhabdopleura are distinctly thinner (25-30 nm according to Dilly 1971). The fusellar fabric in the body of the fusellus in Diplohydra sp. is typical of graptolite fusellar fabric, as defined by Urbanek & Towe (1974: p. 5), i.e. it is a spongy meshwork of interconnecting fibrils (compare also Crowther 1981, pl. 1:6, pl. 4:6). The fuselli of this form closely resemble the simple fuselli of some graptolites because they are composed only of the body and an outer pellicle. The formation of such fuselli may be compared to the Dictyonema type of secretion in Urbanek’s (1976c) classification. On the other hand, the fuselli of both Ordovician forms include straight, unbranched cortical fibrils, parallel to one another, and sometimes closely packed or even cemented. These fibrils may be slightly intermingled with the fusellar fibrils proper. This gradual transition from fusellar fibrils proper to the ordered cortical fibrils in the collar regions of fuselli is fully comparable with a transition from fusellar to cortical fabric within the body of a graptolite fusellus (as described by Urbanek & Towe 1974 and Rickards & Dumican 1984). In the fuselli of some graptolites, these “criss-cross fibrils become more closely packed, forming a layer or lamella of fibrils usually orientated parallel to the circumference of the half-ring”, as Bates & Kirk (1985: p. 210) so clearly showed. Some of their SEM micrographs (especially pl. 2 fig. 12) show a fibril pattern very similar to that of Kystodendron ex gr. longicarpus (Fig 3; see also Bates 1986, fig. 2). Undoubtedly, the fuselli of Kystodendron and Rhabdopleurites may be compared to graptolite fuselli comprising all three fusellar components (i.e. body, pellicle and outer lamella), which are consistent with the Acanthograptus-type of secretion of Urbanek’s (1976c) classification.
The flaky material of Palaeozoic rhabdopleurids described herein has its equivalent in the ultrastructure of some sessile graptolites and should be regarded only as a preservational artifact of normal fibrous material (see below).
So why do our SEM results conflict with Urbanek’s (1976a, b) TEM investigations? Could it be a product of the two very different techniques? SEM microscopy has the advantage that surfaces and fractured sections of the periderm can be examined, whereas TEM microscopy provides only a two-dimensional and very limited field of view. Some TEM-base interpretations of graptolite ultrastructure (e.g. a “ground substance” of the cortical fabric, or the existence and nature of the cortical bandages) have been strongly challenged (e.g. see Crowther & Rickards 1977; Crowther in Urbanek 1978, p. 627; Crowther 1981; Rickards & Dumican 1984), and it can be argued that TEM micrographs may sometimes be positively misleading. Nevertheless, we are of the opinion that the discrepancy in our conclusions and those of Urbanek (1976a, b) is only partly due to the different techniques adopted. It is now possible to reinterpret his micrographs in the light of new ultrastructural data concerning pterobranchs and graptolites.
The fine structure of Ordovician Rhabdopleurites has been crucial to Urbanek’s (1976a, b, 1978, 1986, 1987) arguments which claim that substantial ultrastructural differences exist between the Pterobranchia and the Graptolithina, and that the fibrillar pattern in pterobranch fusellar tissue has changed little since Ordovician times. Thanks to scale bars on Urbanek’s (1976a ,b) micrographs, it is possible to measure fibril diameter. Astonishingly: fibril diameters are generally more than 100 nm and less than 200 nm, which is within the limits of dimensional data measured in the rhabdopleurids described herein. While we share Urbanek’s view that the general arrangement of fibrils in his specimens of Rhabdopleurites is similar to that of living Rhabdopleura, they are unquestionably of graptolite dimensions. It should be stressed that this shape and fibril arrangement is also strikingly similar to the ultrastructural pattern found in some graptolites (e.g. fusellar fibrils of graptoblasts described by Mierzejewski 1984b and Urbanek et al. 1986). The fusellar fibrils of the camaroid graptolite Tubicamara coriacea Koz³owski, 1949 are long, slightly wavy and only rarely seem to be branched (Urbanek & Mierzejewski 1991, fig. 11).. Similar fusellar fibrils were recognized by Urbanek et al. (1982, fig. 14) in the nematularium of the graptoloid Cystograptus vesiculosus (Nicholson).
The Jurassic Rhabdopleura kozlowskii Kulicki, 1969 was the second fossil rhabdopleurid pterobranch studied under the SEM by Urbanek (1976a,b). We agree with him that remarkable differences between its fine structure and that of two living species of Rhabdopleura are a result of fossilization and diagenesis. However, we claim that the fine structure of Rh. kozlowskii reveals distinct similarities to the ultrastructure of some graptolites. The structures recognized by Urbanek (1976b, pl. 4) as matrix of “numerous filamentous materials” distinctly resemble the fusellar fabric of the metasicula of Orthograptus quadrimucronatus Hall, as illustrated under the TEM by Berry & Takagi (1973, fig. 2). On the other hand, the obscure “foamy structures” in the periderm of Rh. kozlowskii may be best compared with the “reticulated fabric” discovered by Urbanek & Mierzejewski (1986) in dendroid graptolites, and with similar structures found in camaroid graptolites (Urbanek & Mierzejewski 1991); these are interpreted as an unusual state of aggregation of the fibrous material. Such “foamy structures” in Jurassic Rhabdopleura are most probably the result of the fusion of originally straight and parallel fibrils, similar to the flaky material identified in three Palaeozoic forms herein. Our preliminary SEM studies of Rh. kozlowskii suggest the presence of heteromorphic fibrillar material in its fusellar tissue and in the wall of a sterile bud cyst (Fig. 8; Mierzejewski & Kulicki, in preparation). In some cases the outer surface of skeletal elements exhibits a complex network of linear features, strikingly similar to poorly preserved graptolite cortical bandages (cf. Crowther & Bergström 1980, pl. 1:3 and Crowther 1981, pl. 19:2). Moreover, we interpret a series of electron-dense membranes on Urbanek’s (1976b, pl. 4C) TEM micrograph as a secondary deposit within the zooidal tubes, recognized by Kulicki (1971) in this species by means of light microscopy. It seems, therefore, that while our SEM observations contradict Urbanek’s (1976a, b) interpretations and conclusions, they are nevertheless consistent with his ultrastructural data.
Our observations also shed a new light on Urbanek’s (1986, 1987) concept of an “ultrastructural anomaly” (see above, p. xxx) and its significance for pterobranch/graptolite taxonomy and phylogeny. Such a supposedly clear distinction at the ultrastructural level between the two groups was not immediately apparent. In the repent tube of living Rhabdopleura compacta Hincks Dilly (1975) found a reticulum of coarse fibres very similar to the fusellar fabric of graptolites. He regarded his discovery as indicative of a close evolutionary origin for cephalodiscids, rhabdopleurids and graptolites (Dilly 1975, 1976). The value of Dilly’s observations and conclusions was underestimated by Urbanek (1976b: p.18; but see also Urbanek 1986: p. 204 and Crowther 1981). Andres (1980) found the fine structure of fusellar tissue in living Rhabdopleura and in an unidentified Ordovician crustoid graptolite to be very similar, but his observations were questioned by Urbanek & Mierzejewski (1984). Crowther (1981: p. 27) observed that “Fusellar fabrics of graptolites and Rhabdopleura bear a superficial resemblance on SEM micrographs”. Mierzejewski (1984b) noted that the apparent structural gap between the fusellar tissue of pterobranchs and the graptolites was partly filled by some unusual fibrils in the periderm of an Ordovician graptoblast (see also Urbanek et al. 1986: p.103, fig. 7A). These fibrils were of cephalodiscid pterobranch ultrastructure, yet of graptolite dimensions. This is consistent with the view of Armstrong et al. (1984) that ultrastructural differences between the skeletel tissues of the Pterobranchia and the Graptolithina are probably less important for phylogenetic considerations than was previously suggested. Mierzejewski’s (1984b) discovery was discussed by Urbanek (1986: p.204, fig. 12A) who considered it “indicative of relative lability between the newly acquired graptolite and the phylogenetically old pterobranch systems of fibrillogenesis”, suggesting that the presence of unusual fibrils “may be explained as biochemical regression to a more primitive stage of fibrillogenesis, owing to the inhibition of growth (...), which disturbs also the processes of fibrillogenesis.” Most significant of all is the case of the Ordovician Pterobranchites antiquus Koz³owski, 1967, which was initially interpreted as a cephalodiscid pterobranch (Koz³owski 1967; Bulman 1970). As stated by Mierzejewski (1984a), this fossil may be regarded as intermediate in form between cephalodiscids and graptolites: all the features of morphological features of its skeleton fall within the limits of variability of the Cephalodiscida, yet the ultrastructure of its periderm (including a typical graptolite-like cortex) appears much closer to graptolites than pterobranchs. In the light of our new observations, the systematic position of the genus Pterobranchites must be reconsidered. Finally, Cephalodiscus solidus Andersson provides further evidence for ‘bridging a gap’ between the ultrastructural organization of the Pterobranchia and the Graptolithina (Dilly, Urbanek & Mierzejewski, unpublished TEM observations), in that some parts of its coenecium are built of a fabric similar to the cortical fabric of graptolites. This fabric comprises long, unbranched fibrils with a translucent core (previously illustrated by Mierzejewski 1984b, pl.16), loosely packed in layers and separated by sheets. In each layer the fibrils are arranged parallel or subparallel, while succesive layers are oriented at different angles. We conclude from all these observations that there is no evidence for an “ultrastructural anomaly”.
The evolution of graptolite skeletal tissues is beyond the scope of this paper, but our work also sheds new light on this problem (addressed previously by, for example, Urbanek 1976c; Andres 1980; Crowther 1981; Rickards et al. 1982; Urbanek & Mierzejewski 1984; Urbanek 1986; Urbanek et al. 1992). Issues include the molecular evolution of collagen and its derivatives within the Pterobranchia and the Graptolithina, fibrillogenesis, corticization, and the origin of the outer lamella in graptolite fuselli. In our view it no longer justifiable to asign the orders of rhabdopleurid pterobranchs (Rhabdopleurida) and sessile graptolites (Camaroidea, Crustoidea, Dendroidea, Tuboidea) to two separate hemichordate classes (i.e. Pterobranchia and Graptolithina) respectively. We agree with Beklemishev (1951) that they should all be treated as members of a single class of the Graptolithoidea (see also Urbanek 1986, 1994). Finally, our investigations have created a new ‘Problem Situation’ for the debate on graptolite affinities, as defined by Urbanek (1986, 1987). Continuing Urbanek’s historical sequence (PS 1-10), PS 11 may be called rejection of the concept of the ‘ultrastructural anomaly’.
(i) The fine structure of fusellar tissue in Palaeozoic rhabdopleurid pterobranchs is distinct from that of Recent Pterobranchia; there are differences in shape, dimensions and arrangement of the fusellar fibrils. Recent Rhabdopleura and Cephalodiscus have their fusellar tissue made exclusively of thin (20-30 nm) needle-like fibrils loosely dispersed in matrix, whereas fibrils of fossil pterobranchs are of two categories: (1) fusellar fibrils proper, distinctly thicker (70-150 nm in diameter), often branched/anastomosed, forming a solid three-dimensional spongy network; and sometimes, (2) cortical fibrils, thicker still (usually 150-200 nm in diameter), straight, unbranched and forming band-like constructions.
(ii) There is little to separate graptolites from fossil rhabdopleurid pterobranchs in the fusellar component of their skeleton. Thus, contrary to Urbanek (1986, 1987), the so-called ‘ultrastructural anomaly’ is not diagnostic of the graptolite grade of rhabdosome construction because there is no such anomaly among Palaeozoic forms. The fusellar tissue of both groups is made predominantly of fusellar fibrils sensu stricto forming a spongy meshwork of anastomosing/branching fibrils, sometimes accompanied by ordered cortical fibrils.
(iii) This heteromorphy of fibrous material (a three-dimensional network composed of anastomosing/branching fibrils, with fragments of fuselli built up of ordered fibrils) is not unique to graptolites. Such features were presumably attained by the common ancestor of pterobranchs and graptolites.
(iv) There is no now reason to regard pterobranchs and graptolites as two separate classes of the phylum Hemichordata. We share Beklemishev’s (1951, 1970) opinion that they should be treated as members of one class - the Graptolithoidea.
The present authors are grateful to Professor A. Urbanek (Poland) for a careful reading of the manuscript and helpful criticism. Dr. P.R. Crowther and Professor P.N. Dilly (both U.K.) as referrees made a number of helpful remarks. Special thanks are due to Dr. A. Mørk and Dr. H.A. Nakrem (both Norway), as well as to Professor H. Szaniawski (Poland) for making specimens of Diplohydra sp. available for the present study. The core material with Diplohydra sp. was drilled during the Continental Shelf Institute (IKU – Trondheim) Barents Sea Program.
Andres, D. 1977. Graptolithen aus ordovizischen Geschieben und die frühe Stammesgeschichte der Graptolithen. – Paläontologische Zeitschrift 51, 52-93.
Andres, D. 1980. Feinstrukturen und Verwandtschaftsbeziehungen der Graptolithen. – Paläontologische Zeitschrift 54, 129-170.
Armstrong, W.G., Dilly, P.N. & Urbanek, A. 1984. Collagen in the pterobranch coenecium and the problem of graptolite affinities. – Lethaia 17, 145-152.
Bates, D.E.B. & Kirk, N.H. 1985. Graptolites, a fossil case-history of evolution from sessile, colonial animals to automobile superindividuals. – Proceedings of Royal Society of London B 228, 207-224.
Bates, D.E.B. 1986. The construction of graptolite rhabdosomes in the light of ultrastructural studies. – Indian Journal of Geology 59, 1-28.
Bates, D.E.B. 1997. The ultrastructure of a Silurian dendroid from Gotland (Sweden). – Geobios 20, 27-37.
Beklemishev, V.N. 1951. K postroeniyu sistemy zhivotnykh. Vtorichnorotye (Deuterostomia), ikh proizkhozdenie i sostav. - Uspekhi Sovremennoy Biologii 32, 256-270.
Beklemishev, V.N. 1970 (Russian ed. 1951, 1964). Principles of Comparative Anatomy of Invertebrates, vol. 1, 490 pp.; vol. 2, 529 pp. Oliver and Boyd, Edinburgh.
Bohlin, B. 1949. The Asaphus limestone in northernmost Öland. - Bulletin of the Geological Institutions of the University of Uppsala 33, 529-570.
Bohlin, B. 1950. – The affinities of graptolites. – Bulletin of the Geological Institutions of the University of Uppsala 34, 107-113.
Chapman, A.J., Durman, P.N, & Rickards, R.B. 1996. A provisional classification of the graptolite Order Dendroidea. – Paläontologische Zeitschrift 70, 189-202.
Crowther, P.R.1978. The nature and mode of life of the graptolite zooid with reference to secretion of the cortex. – Acta Palaeontologica Polonica 23, 473-479.
Crowther, P.R. 1981. The fine structure of graptolite periderm. – Special Papers in Palaeontology 26, 1-119.
Crowther, P.R. & Bergström, S.M. 1980. Cortical bandages in an Upper Ordovician glyptograptid graptolite from Ohio. – Bolletino della Societa Paleontologica Italiana 19, 250-253.
Crowther, P.R. & Rickards, R.B. 1977. Cortical bandages and the graptolite zooid. – Geologia et Palaeontologica 11, 9-46.
Decker, C.E. 1956. Place of graptolites in animal kingdom. – Bulletin of the American Association of Petroleum Geology 40, 1699-1704.
Dilly, P.N. 1971. Keratin-like fibres in the Hemichordate Rhabdopleura compacta. – Zeitschrift für Zellforschungen 117, 502-515.
Dilly, P.N. 1975. The dormant buds of Rhabdopleura compacta (Hemichordata). – Cell and Tissue Research 159, 387-397.
Dilly, P.N. 1976. Some features of the ultrastructure of the coenecium of Rhabdopleura compacta. - Cell and Tissue Research 170, 253-261.
Dilly, P.N. 1993. Cephalodiscus graptolitoides sp.nov. a probable extant graptolite. – Journal of Zoology 229, 69-78.
Grahn, Y. 1980. Early Ordovician Chitinozoa from Öland. – Sveriges geologiska undersökning C, 775, 1-41.
Hyman, L.H. 1959. The Invertebrates.V. Smaller Coelomate Groups. McGraw-Hill, New York, 783 pp.
Kirk, N.H. 1972. Some thoughts on the construction of the rhabdosome in the Graptolithina, with special reference to extrathecal tissue and its bearing on the theory of automobility. – Publications of the Department of Geology, University College of Wales, Aberystwyth 1, 1-21.
Kirk, N.H. 1974. More thoughts on the construction of the rhabdosome in the Dendroidea and of Mastigograptus. – Publications of the Department of Geology, University College of Wales, Aberystwyth 6, 1-11.
Kirk, N.H. 1975. More thoughts on the construction and functioning of the rhabdosome in the Graptolithoidea in the light of their ultrastructure. – Publications of the Department of Geology, University College of Wales, Aberystwyth 7, 1-21.
Koz³owski, R. 1938. Informations preliminaires sur les Graptolithes du Tremadoc de la Pologne et sur leur portee theorique.- Annales Musei Zoologici Polonici 13, 183-196.
Koz³owski, R. 1949. Les graptolithes et quelques nouveaux groupes d’animaux du Tremadoc de la Pologne. – Palaeontologia Polonica 3, i-xii, 1-239.
Koz³owski, R. 1966. On the structure and relationships of graptolites. –Journal of Paleontology 40, 489-501.
Koz³owski, R. 1967. Sur certains fossiles ordoviciens à test organique. –Acta Palaeontologica Polonica 12, 99-132.
Koz³owski, R. 1970. Nouvelles observations sur les Rhabdopleurides (Pterobranchia) ordoviciens. –Acta Palaeontologica Polonica 15, 3-17.
Kulicki, C. 1969. The discovery of Rhabdopleura (Pterobranchia) in the Jurassic of Poland. – Acta Palaeontologica Polonica 14, 537-552.
Kulicki, C. 1971. New observations on Rhabdopleura kozlowskii (Pterobranchia) from the Bathonian of Poland. – Acta Palaeontologica Polonica 16, 415-429.
Mierzejewski, P. 1977. The first discovery of Crustoidea (Graptolithina) and Rhabdopleurida (Pterobranchia) in the Silurian. – Bulletin de l‘Académie Polonaise des Sciences. Série des Sciences de la Terre 25, 103-107.
Mierzejewski, P. 1984a. Pterobranchites Koz³owski, 1967 – an aberrant graptolite ? – Acta Palaeontologica Polonica 29, 83-89.
Mierzejewski, P. 1984b. Cephalodiscus-type fibrils in the graptoblast fusellar tissue. – Acta Palaeontologica Polonica 29, 157-160.
Mierzejewski, P. 1986. Ultrastructure, taxonomy and affinities of some Ordovician and Silurian organic microfossils. – Palaeontologia Polonica 46, 129-220.
Nakrem, H.A., Szaniawski, H. & Mørk, A. (2001). Permian-Triassic scolecodonts and conodonts from the Svalis Dome, central Barents Sea, Norway. –Acta Palaeontologica Polonica 46.
Nilsson. I., Mangerud, G. & Mørk, A. 1996. Permian stratigraphy of the Svalis Dome, south-western Barents Sea.-Norsk Geologisk Tidsskrift 76, 127-146.
Rickards, R.B. 1975. Palaeoecology of the Graptolithina, an extinct Class of the Phylum Hemichordata. – Biological Review 50, 397-436.
Rickards, R.B., Chapman, A.J. & Temple, J.T. 1984. Rhabdopleura hollandi, a new pterobranch hemichordate from the Silurian of the Llandovery district, Powys, Wales. – Proceedings of the Geologists‘ Association 95, 23-28.
Rickards, R.B. & Crowther, P.R. 1978. New observations on the mode of life, evolution and ultrastructure of graptolites. – In: Systematics Association Special Volume 2, G. Larwood & B.R. Rosen (eds) “Biology and systematics of colonial organisms“. Academic Press, London and New-York, 397-410.
Rickards, R.B. & Dumican, L.W. 1984. The fibrillar component of the graptolite periderm. – Irish Journal of Earth Sciences 6, 175-203.
Skevington, D. 1965. Graptolites from the Ontikan limestones Ordovician of Öland, Sweden. II. Graptoloidea and Graptovermida.- Bulletin of the Geological Institutions of the University of Uppsala 43, 1-74.
Towe, K.M. & Urbanek, A. 1972. Collagen-like structure in Ordovician graptolite periderm. – Nature 237, 443-445.
Urbanek, A. 1976a. The problem of graptolite affinities in the light of the ultrastructure of the periderm in Dendroidea and Pterobranchia. In: Evolutionary Biology, 205-211. Praha.
Urbanek, A. 1976b. The problem of graptolite affinities in the light of ultrastructural studies on peridermal derivatives in pterobranchs. – Acta Palaeontologica Polonica 21, 3-36.
Urbanek, A. 1976c. Ultrastructure of microfuselli and the evolution of graptolite skeletal tissues. – Acta Palaeontologica Polonica 21, 315-331.
Urbanek, A. 1978. Significance of ultrastructural studies for graptolite research. – Acta Palaeontologica Polonica 23, 595-629.
Urbanek, A. 1986. The enigma of graptolites ancestry: Lesson from a phylogenetic debate. In: A. Hoffman & M.H. Nitecki (eds), Problematic Fossil Taxa, 184-226, Oxford University Press, New York Clarendon Press, Oxford.
Urbanek, A. 1987. The phylogenetic debate on the affinities of graptolites. An attempt at a methodological analysis. – Bulletin of the Geological Society of Denmark 35, 22-230.
Urbanek, A. 1994. When is a pterobranch a graptolite? – Lethaia 27, 324.
Urbanek, A. & Dilly, P.N. (2000). The stolon system in Rhabdopleura compacta and its phylogenetic implications. – Acta Palaeontologica Polonica 45, 201-226.
Urbanek, A. & Mierzejewski, P. 1984. The ultrastructure of the Crustoidea and the evolution of graptolites skeletal tissues. – Lethaia 17, 73-91.
Urbanek, A. & Mierzejewski, P. 1986. A possible new pattern of cortical deposit in Tremadoc dendroid graptolites from chert nodules. – In: Hughes, C.P. & Rickards, R.B. (eds), Palaeoecology and biostratigraphy of graptolites, Geological Society Special Publication 20, 13-19.
Urbanek, A. & Mierzejewski, P. 1991. The fine structure of a camaroid graptolite. – Lethaia 24, 129-137.
Urbanek, A., Mierzejewski, P. & Bengtson, S. 1992. Fine structure of the earliest known rhabdopleurid. – Lethaia 25, 349-350.
Urbanek, A., Mierzejewski, P. & Rickards, B. 1986. New observations on the fine structure of graptoblasts. – Lethaia 19, 97-107.
Urbanek, A. & Towe, K.M. 1974. Ultrastructural studies on graptolites, 1: The periderm and its derivatives in the Dendroidea and in Mastigograptus. – Smithsonian Contributions to Paleobiology 20, 1-48.
Fig. 1. Kystodendron ex gr. longicarpus (Eisenack). Lower Llanvirn (Ontikan Limestones of the Valaste age), Gilbergabrottet 1, Öland (Sweden). SEM micrographs. Specimen consisting of erect tube and incompletely preserved creeping tube (ZPAL Pb/0/1). A. Lateral view of the specimen; x 110. B. Distal part of the erect tube; x 550. C. Upper surface of the margnal memebrane; x 3500. Abbreviations: c – collar of fusellus, ct – creeping tube, et – erect tube, f – fusellus, m – marginal membrane, o – oblique suture of fuselli.
Fig. 2. Kystodendron ex gr. longicarpus (Eisenack). Lower Llanvirn (Ontikan Limestones of Valaste age), Gilbergabrottet 1, Öland (Sweden) ZPAL Pb/0/1. Well-preserved outer surface of fusellar increments; ca x2000. SEM micrograph. Abbreviations: f – fusellus, c – collar of fusellus, o – oblique suture of fuselli.
Fig. 3. Kystodendron ex gr. longicarpus (Eisenack). Lower Llarnvirn (Ontikan Limestones of Valaste age), Gilbegrabrottet 1, Öland (Sweden). SEM micrographs. ZPAL Pb/0/1. Fine structure of fusellar collars. A. X ca 5500. B. x ca 5500. C. x 21000 Abbreviations: c – collar of fusellus, cf – cortical fibril, of – outer pellicle of fusellus, d – debris of peeled off pellicle, ff – fusellar fibrils proper, m – margin of fusellar collar, p – delicate periderm reflecting underlying fusellar fibrils.
Fig. 4. Kystodendron ex gr. longicarpus (Eisenack). Lower Llanvirn (Ontikan Limestones of Valaste age), Gilbergabrottet 1, Öland (Sweden). SEM micrographs. ZPAL Pb/0/1. Anastomosing and/or branching fusellar fibrils proper intermingled with flakes. A. ca x 21000. B. ca x 21000. C x 21000. Abbreviations: ff – fusellar fibril, fk – flake.
Fig. 5. Rhabdopleurites primaevus Koz³owski, 1967. Lower Llanvirn (Ontikan Limestones of Valaste age), Gilbergabrottet 1, Öland (Sweden). SEM micrographs. ZPAL Pb/0/2. A. Fragment of the strongly flattened zooidal tube; x 90. B. Surface of the periderm; x 5200. Abbreviations: fc - fusellar collar, pa – “patch”.
Fig. 6. Rhabdopleurites primaevus Koz³owski, 1967. Lower Llanvirn (Ontikan Limestones of Valaste age), Gilbergabrottet 1, Öland (Sweden). ZPAL Pb/0/2. SEM micrograph showing fine structure of the fusellar tissue. x 15500. Abbreviations: c – fusellar collar, cf – cortical fibril, ff – fusellar fibril, fk – flake.
Fig. 7. Diplohydra sp. Kazanian (Upper Permian), core Dia 84-31 (sample P3, depth 10.18-10.40 m), Svalis Dome, central Barents Sea (Norway). SEM micrographs.A. Flake material from the fusellar tissue with indinstinct traces of fusellar fibrils and numerous meshes. x 5500, ZPAL Pb/0/4 B. Fibrous material covering the outer surface of the stolon. x 19500, ZPAL Pb/0/5.
Fig. 8. Rhabdopleura kozlowskii Kulicki, 1969. Callovian (Jurassic), £apiguz clay pit, £uków (Poland). SEM micrographs. ZPAL Pb/0/6. A. Fragment of a zooidal tube. x 210. B. Fissure in the periderm; arrow indicates a presumably bunch of cortical fibrils. x 14000. C. Unconformity between two presumably bunches of cortical fibrils on the surface of a sterile bud cyst. Note a striking similarity to cortical bandages in graptolites! x 14300.