Hostname: page-component-74656f9884-2dmjx Total loading time: 0 Render date: 2026-11-08T10:49:04.614Z Has data issue: false hasContentIssue false
  • English
  • Français

Emergence, biodiversification and extinction of the chitinozoan group

Published online by Cambridge University Press:  07 July 2010

YNGVE GRAHN  and
FLORENTIN PARIS
YNGVE GRAHN*
Affiliation:
Universidade do Estado do Rio de Janeiro, Faculdade de Geologia, Bloco A – Sala 4001, Rua São Francisco Xavier 524, 20550-013 Rio de Janeiro, R.J., Brazil
FLORENTIN PARIS
Affiliation:
Université de Rennes 1, Géosciences Rennes, UMR 6118 du CNRS, 35042 Rennes-cedex, France
*
*Author for correspondence: yngvegrahn@gmail.com
Rights & Permissions [Opens in a new window]

Abstract

Chitinozoans are considered as reproductive bodies of marine invertebrates, called chitinozoophorans. These chitinozoophorans were most likely to have been small, pelagic or necto-pelagic, soft-bodied, probably wormlike animals, and judging from the size of chitinozoans, they probably measured from a few millimetres to a few centimetres in length. The chitinozoophorans most likely survived by grazing on phytoplankton. There is no evidence of a large colonization of the pelagic niche in the Cambrian, but from the Early Ordovician onward, this niche was exploited chiefly by graptolites and chitinozoophorans. Both groups inhabited nearshore and offshore habitats, but in contrast to the graptolites, the chitinozoans displayed their highest diversity at high latitude, in less distal (that is, upper and lower offshore) environments. The chitinozoan group evolved rapidly during the Ordovician and reached its maximum Ordovician diversity in the late Darriwilian. From the first occurrence of chitinozoans in early Tremadocian times, to the biodiversity crisis in latest Ordovician times, nearly 80 % of the morphological innovations took place. Until their extinction in the latest Devonian, chitinozoans survived through several biodiversity crises: in the early Late Ordovician, late Hirnantian, late Wenlock, earliest Emsian, and in the latest Frasnian (Kellwasser event). During the melting of the Hirnantian ice sheet, most Ordovician genera and species became extinct, but some genera extended beyond the boundary (e.g. Spinachitina, Belonechitina, Cyathochitina, Ancyrochitina). The Hirnantian glaciation was not directly responsible for the dramatic extinction of organic-walled microfossils, but it certainly accelerated the extinction of lineages that had already been weakened since the early to mid-Katian. The late Wenlock and earliest Emsian graptolite crises affected the chitinozoophorans to a lesser degree, and the latest Frasnian Kellwasser event did not greatly affect chitinozoophorans. The disappearance of the chitinozoan group at the end of the Famennian resulted from a combination of factors, for example, the chitinozoophorans probably no longer had the genetic potential for successful adaptations to successive drastic environmental changes (only one species is known from the latest Famennian), their usual niche was invaded by more efficient groups, and their usual food supply disappeared or was no longer sufficient. The latter factor is supported by the contemporaneous decline in phytoplankton.

Keywords

Chitinozoapalaeobiodiversityextinction eventsEarly Palaeozoic

Information

Type
Original Article
Information
Geological Magazine , Volume 148 , Issue 2 , March 2011 , pp. 226 - 236
Copyright
Copyright © Cambridge University Press 2010

1. Introduction

The various shapes of chitinozoan vesicles (e.g. discoidal, spherical, tubular, conical, etc.) are commonly represented in numerous unrelated fossil and extant unicellular organisms or reproductive cycles of metazoans. Thus, chitinozoan affinities based on shape have led to numerous radically different biological assignments (for a discussion, see Paris et al. Reference Paris, Grahn, Nestor and Lakova1999). The inferred chitinous composition of the chitinozoan vesicle wall was used by Eisenack (Reference Eisenack1931, Reference Eisenack1968), Collinson & Schwalb (Reference Collinson and Schwalb1955) and Jenkins (Reference Jenkins1970) to support particular inferred biological affinities. However, Voss-Foucart & Jeuniaux (Reference Voss-Foucart and Jeuniaux1972) and Jacob et al. (Reference Jacob, Paris, Monod, Miller, Tang, George and Bény2007) were unable to establish the presence of chitin in the organic vesicle wall. This presents two possibilities: (1) that the molecular structure of chitin is not preserved through geological time or (2) the wall of chitinozoan vesicles contained no chitin. The available data do not allow us to establish which is correct (Jacob et al. Reference Jacob, Paris, Monod, Miller, Tang, George and Bény2007).

Kozlowski (Reference Kozlowski1963) was the first to use the mode of chitinozoan aggradation in biological affinity arguments. Specimens of the genus Desmochitina Eisenack Reference Eisenack1931, which were contained within an organic-walled cocoon, were considered by Kozlowski to be similar to polychaete eggs enclosed in a similar structure. However, the various types of attachments to form chains or other types of vesicle aggregation cannot be evaluated for their biological affinity significance, since many invertebrates display a similar mode of egg laying.

Grahn (Reference Grahn1981) named the supposed marine metazoan parent organisms ‘chitinozoophorans’, and considered chitinozoans to be the reproductive bodies of a marine invertebrate. Paris (Reference Paris1981) discussed the possibility of small, pelagic or nectic, soft-bodied, wormlike (judging from the elongate coiled chains) animals as the parent organism, and based on the size of the chitinozoans, deduced that these would range from a few millimetres to a few centimetres in length. The distribution and biodiversification pattern of the chitinozoans may not exactly reflect those of the chitinozoophorans. A pelagic or necto-pelagic animal may use different strategies (see Paris & Nõlvak, Reference Paris and Nõlvak1999) in laying its eggs: (1) the eggs were freely spread in the water, or (2) they were attached to floating objects (e.g. seaweed) or the chitinozoophorans attached their eggs to any object that offered protection (e.g. Grahn, Reference Grahn1984b). It is likely that two modes of occurrence could be expected for such eggs in a fossil state: (1) evidence of eggs before laying, that is, the ‘intra-oviduct stage’ (e.g. frequently coiled chains persisted after the decay of the females; see Paris & Nõlvak, Reference Paris and Nõlvak1999; fig. 3), and (2) evidence of eggs after laying (cocoons, organized clusters, isolated vesicles). The chitinozoan vesicles were probably surrounded by a mucous or gelatinous layer (e.g. Paris & Nõlvak, Reference Paris and Nõlvak1999; fig. 4). This is corroborated by the occurrence of a chain of Lagenochitina esthonica Eisenack, Reference Eisenack1955, found in Tremadocian beds from England (Y. G., unpub. data), which was surrounded by framboidal pyrite where a mucous or gelatinous layer could be expected. Soft tissues, even of a gelatinous nature, are known to be frequently preserved through alteration of organic sulphur compounds to pyrite (Stanley & Sturmer, Reference Stanley and Sturmer1983). An important condition for such preservation is a quick burial, preferably in organic-rich sediments (Brett & Baird, Reference Brett and Baird1986). These clusters should not be confused with secondary stacking (e.g. faecal pellets, stuck vesicles, etc.).

Chitinozoans evolved rapidly during Ordovician times. From their first occurrence in the early Tremadocian to the biodiversity crisis in the latest Ordovician, nearly 80 % of morphological innovations took place (Paris & Nõlvak, Reference Paris and Nõlvak1999; Paris et al. Reference Paris, Grahn, Nestor and Lakova1999). Chitinozoans had already reached their maximum Ordovician diversity by the late Darriwilian (Fig. 1). Until their extinction in latest Devonian times, the chitinozoan group survived several biodiversity crises: in the early Late Ordovician (Paris et al. Reference Paris, Achab, Asselin, Chen, Grahn, Nõlvak, Obut, Sennikov, Vecoli, Verniers, Wang, Winchester-Seeto, Webby, Paris, Droser and Percival2004), late Hirnantian, late Wenlock, earliest Emsian, and in the latest Frasnian (Kellwasser event). The general trend through time is shown in Figure 1.

Figure 1.

Global evaluation of the chitinozoan biodiversification from the origin of the group in the early Tremadocian to its extinction in the latest Devonian. The solid circles indicate the number of species per stage (Ordovician and Devonian) or per series (Silurian). The graph represents the mean diversity of the chitinozoans per million years for the stages or series (durations based on Sadler, Cooper & Melchin, Reference Sadler, Cooper and Melchin2009). An alternative graph (dashed line) is based on the time calibration by Ogg, Ogg & Gradstein (Reference Ogg, Ogg and Gradstein2008). The most significant events are indicated along the time scale. Open arrow: Darriwilian cooling (Trotter et al. Reference Trotter, Williams, Barns, Lécuyer and Nicoll2008; Ainsaar et al. Reference Ainsaar, Kaljo, Martma, Meidla, Männik, Nõlvak and Tinn2010); black arrow: biological and oceanological events (Jaeger, Reference Jaeger1978, Reference Jaeger1991; Meyer-Berthaud, Scheckler & Wendt, Reference Meyer-Berthaud, Scheckler and Wendt1999; House, Reference House2002; Joachimski et al. Reference Joachimski, Pancost, Freeman, Ostertag-Henning and Buggisch2002; Kaljo et al. Reference Kaljo, Hints, Männik and Nõlvak2008; Servais et al. Reference Servais, Lehnert, Li, Mullins, Munnecke, Nützel and Vecoli2008; Bergström et al. Reference Bergström, Chen, Gutiérrez-Marco and Dronov2009a; Hints et al. Reference Hints, Delabroye, Nõlvak, Servais, Uutela and Wallin2010); black star: main anoxic events (Chlupáč & Kukal, Reference Chlupáč and Kukal1988; House, Reference House2002); circled star: main glacial events (Streel et al. Reference Streel, Caputo, Loboziak and Melo2000; Lehnert et al. Reference Lehnert, Männik, Joachimski, Calner and Fryda2010). The values of the biodiversity of the chitinozoan at species level are from the database ‘CHITINOVOSP’ of F. Paris.

The occurrence of chitinozoans in all types of sedimentary rocks (except for reefs and coarse, well-sorted sandstones), including black shales and cherts devoid of any bioturbation or evidence of benthic fauna, suggests that the chitinozoophorans were, most likely, part of the zooplankton (Vandenbroucke et al. Reference Vandenbroucke, Armstrong, Williams, Paris, Sabbe, Zalasiewicz and Nõlvak2010). It is probable that chitinozoophorans grazed on phytoplankton. This pelagic niche appeared in the Cambrian (Servais et al. Reference Servais, Lehnert, Li, Mullins, Munnecke, Nützel and Vecoli2008), but was only exploited from the Early Ordovician onward. It was also occupied by graptolites, which appeared a little earlier in the fossil record than chitinozoophorans (Cooper, Reference Cooper1999). However, the specific diversities of these two groups are inverted with relation to climatic belts: intertropical zones were dominated by highly diversified graptolite faunas and higher latitudes by chitinozoophorans. This is demonstrated for the early Sandbian by Vandenbroucke et al. (Reference Vandenbroucke, Armstrong, Williams, Paris, Sabbe, Zalasiewicz and Nõlvak2010). These authors also concluded that graptolites and chitinozoophorans did not share exactly the same ecosystem.

The fluctuation of the diversity of the chitinozoans through time, from the origination of the group in the early Tremadocian, to its final extinction in the latest Famennian, was evaluated using the ‘CHITINOVOSP’ database initiated by Paris & Bernard (Reference Paris, Bernard and Dorning1994) and updated by one of us (F. P.). All chitinozoan species described since Eisenack's first species description in 1931 are recorded in this database (1214 species). Besides the various taxonomic form fields, the database also includes palaeogeographic and stratigraphic information. The latter entries contain the total range of the recorded species at System, Series and Stage levels. The database has been periodically updated and the last international subdivisions adopted by IUGS are used (that is, the most recent Ordovician global stages).

The number of species per stage can be found by querying the database. These numbers should be regarded as approximate values, as the total range of each species is often a matter of estimation, related to the accuracy of the available stratigraphic information. In addition, ill-defined species included in the database add some further bias. Nevertheless, as the same treatment has been applied throughout the Palaeozoic record of chitinozoan species, the resulting general trends seem to reflect fairly well the actual biodiversification pattern of the group (Fig. 1), as supported by detailed sections providing a well-documented diversity trend for some short time intervals.

The durations of the Wenlock and Ludlow stages as calculated by Sadler, Cooper & Melchin (Reference Sadler, Cooper and Melchin2009) are much shorter than the duration of the Ordovician and Devonian stages. Consequently, in order to have a time slice roughly in the same range, the chitinozoan specific diversity is expressed at series level for Wenlock and Ludlow on Figure 1. However, a more detailed graph is provided for the Silurian (Fig. 2) with specific diversity also evaluated at stage level for the Wenlock and the Ludlow. This different time slicing points out a drop in diversity in the Homerian roughly contemporaneous with the late Wenlock graptolite crisis (see the lundgreni event in Section 5). The two graphs also illustrate the great influence of the time slicing on the diversity curves.

Figure 2.

Global biodiversity of the Silurian chitinozoans species per stage (solid circles) and mean value of their specific diversity per million years for each stage. (Numerical calibration from Sadler, Cooper & Melchin, Reference Sadler, Cooper and Melchin2009.)

Some discrepancies are noted when calibrating chronostratigraphic subdivisions with the most recent numerical scales. The mean chitinozoan diversity per million years shows higher values for the Darriwilian, the Aeronian and the Pridoli, when using the numerical calibration of Ogg, Ogg & Gradstein (Reference Ogg, Ogg and Gradstein2008), with regard to those proposed by Sadler, Cooper & Melchin (Reference Sadler, Cooper and Melchin2009). However, these different calibrations do not introduce significant bias, as the general trends of the resulting graphs are similar (Fig. 1). As demonstrated by a more detailed evalution of the diversity of Ordovician chitinozoans (Paris et al. Reference Paris, Achab, Asselin, Chen, Grahn, Nõlvak, Obut, Sennikov, Vecoli, Verniers, Wang, Winchester-Seeto, Webby, Paris, Droser and Percival2004), one of the critical points when elaborating such curves is the unbalanced quality of the available data; for instance, some time slices and some areas have been more extensively investigated than others (e.g. the diversity curve tends to mirror the number of available samples; see Paris et al. Reference Paris, Achab, Asselin, Chen, Grahn, Nõlvak, Obut, Sennikov, Vecoli, Verniers, Wang, Winchester-Seeto, Webby, Paris, Droser and Percival2004, fig. 28.2–3) and this must be kept in mind when discussing diversity fluctuations.

2. The emergence of the chitinozoan group

The first chitinozoans appear during a transgression event with shaly facies above the Cambrian sandstones and after the negative TOCE (Top of Cambrian Excursion) δ13C curve (Zhu, Badcock & Peng, Reference Zhu, Badcock and Peng2006). The chitinozoophorans colonized the niche as pelagic zooplankton together with dendroid graptolites (e.g. Dendrograptids, Anisograptids) and then with the first graptoloids. No undisputable chitinozoans have been recorded before the Ordovician, and the microfossils reported as chitinozoans from the Neoproterozoic Chuar Group by Bloeser et al. (Reference Bloeser, Scopf, Hordystir and Breed1977) are most probably testate amoebas (Porter & Knoll, Reference Porter and Knoll2000; Porter, Meisterfeld & Knoll, Reference Porter, Meisterfeld and Knoll2003). Simple, smooth, quite large chitinozoan forms (Lagenochitina, Conochitina) appear in the early Tremadocian. They are known from the middle part of the Fezouata Formation in Morocco (Elaouad-Debbaj, Reference Elaouad-Debbaj1988), where the first known chitinozoans (Lagenochitina destombesi) occur below the Adelograptus tenellus graptolite Zone, and above early Tremadocian taxa (Destombes, Holland & Willefert, Reference Destombes, Holland, Willefert and Holland1985; Paris, Reference Paris1990). Early Tremadocian chitinozoans have also been reported from the Yangtze area in south China (Chen, Paris & Zhang, Reference Chen, Paris and Zhang2008). During the late Tremadocian, chitinozoans spread to areas outside north Gondwana, and the morphological diversification now also includes species with smaller vesicles (Desmochitina, Euconochitina), together with large specimens from the Lagenochitina esthonica group. Early late Tremadocian (Adelograptus tenellus graptolite Zone) chitinozoans have been reported from the upper El Gassi Formation in Algeria (Poumot, Reference Poumot1964, Reference Poumot1968; Combaz, Reference Combaz1967; Videt et al. Reference Videt, Paris, Rubino, Boumendjel, Dabard, Loi and Ghienne2010) and from the New Fields Farm borehole (908.15 m), 5 km west of Southam, Warwickshire, England (Y. G., unpub. data). De la Puente & Rubinstein (Reference De la Puente and Rubinstein2009) described Lagenochitina from the Aorograptus victoriae graptolite Zone (Saladillo Formation), and chitinozoans from the lower Parsha Formation, Argentina. Chen, Paris & Zhang (Reference Chen, Paris and Zhang2008) reported Lagenochitina destombesi from the late Tremadocian in the Yichang area (Fenxiang Formation), Hubei Province, China. The same species has been recovered from the Varangu regional stage of Estonia (Nõlvak, Reference Nõlvak1999). During the latest Tremadocian, chitinozoophorans expanded to all the paleocontinents, for example, the upper Cienguillas and lower Obispo formations, east Codillera, Bolivia (Heuse, Grahn & Erdtmann, Reference Heuse, Grahn and Erdtmann1999), and the Montagne Noire/Aquitaine Basin, southwest France (Paris, Reference Paris1984). Outside Gondwana they are known from a number of places such as the Björkåsholmen Formation in Skåne, south Sweden (Nõlvak & Grahn, Reference Nõlvak and Grahn1993; Grahn & Nõlvak, Reference Grahn and Nõlvak2010), Oslo Region, south Norway (Grahn & Nõlvak, Reference Grahn and Nõlvak2007a), and Isle of Rügen, NE Germany (Samuelsson, Reference Samuelsson, Kraft and Fatka1999); Leetse Formation, Estonia (Grahn, Reference Grahn1984a; Hints & Nõlvak, Reference Hints and Nõlvak2006); Cow Head, Ledge Section, Newfoundland, Canada (Williams et al. Reference Williams, Nowlan, Barnes and Batten1999); and Altai, Siberia (Sennikov et al. Reference Sennikov, Yolkin, Petrunina, Gladkikh, Obut, Izokh, Kipriyanova, Sennikov and Kanygin2008).

3. Chitinozoan maximum diversity in the late Darriwilian

The chitinozoophorans quickly expanded during Early and Middle Ordovician times (Fig. 1), and reached their maximum Ordovician diversity (only to be exceeded in the early Wenlock and Pridoli) in the late Darriwilian (Paris & Nõlvak, Reference Paris and Nõlvak1999; Paris et al. Reference Paris, Grahn, Nestor and Lakova1999, Reference Paris, Achab, Asselin, Chen, Grahn, Nõlvak, Obut, Sennikov, Vecoli, Verniers, Wang, Winchester-Seeto, Webby, Paris, Droser and Percival2004; Hints et al. Reference Hints, Delabroye, Nõlvak, Servais, Uutela and Wallin2010) after about 15 Ma. The genetic potential was probably high with a ‘plasticity’ of the genome of the chitinozoophorans favouring new combinations (Paris et al. Reference Paris, Achab, Asselin, Chen, Grahn, Nõlvak, Obut, Sennikov, Vecoli, Verniers, Wang, Winchester-Seeto, Webby, Paris, Droser and Percival2004). The sea-levels were rising, but in the late Darriwilian a short lived regression (Dabard, Loi & Paris, Reference Dabard, Loi and Paris2007) occurred with the onset of a cooler climate (Trotter et al. Reference Trotter, Williams, Barns, Lécuyer and Nicoll2008; Ainsaar et al. Reference Ainsaar, Kaljo, Martma, Meidla, Männik, Nõlvak and Tinn2010). The regression and the climate change affected chitinozoophorans, and chitinozoan diversity decreased until a recovery in the Katian (Fig. 1).

4. The Hirnantian/Rhuddanian biodiversity crisis

The first major biodiversity crisis for chitinozoophorans on a global basis coincides with the Guttenberg δ13C excursion (GICE) in the early Late Ordovician (Paris & Nõlvak, Reference Paris and Nõlvak1999; Paris et al. Reference Paris, Achab, Asselin, Chen, Grahn, Nõlvak, Obut, Sennikov, Vecoli, Verniers, Wang, Winchester-Seeto, Webby, Paris, Droser and Percival2004; Achab & Paris, Reference Achab and Paris2007; Bergström et al. Reference Bergström, Chen, Gutiérrez-Marco and Dronov2009a, Reference Bergström, Chen, Schmitz, Young, Rong and Saltzmanb). The decline in chitinozoan species diversity (Fig. 1) is in general connected with decreases in sea-level, most likely caused by the development of restricted intra-continental ice sheets (Hamoumi, Reference Hamoumi1999; Ainsaar, Meidla & Martna, Reference Ainsaar, Meidla and Martna2004; Bourahrouh, Paris & Elaouad-Debbaj, Reference Bourahrouh, Paris and Elaouad-Debbaj2004; Loi et al. Reference Loi, Ghienne, Dabard, Paris, Botquelen, Christ, Elaouad-Debbaj, Gorini, Vidal and Videt2010), or by increased tectonic activity. Subsequently, a change in sedimentation led to a positive change in δ13C, extinction, and a microfaunal crisis. Glaciation pulses leading to the Hirnantian glaciation (Bergström, Saltzman & Schmitz, Reference Bergström, Saltzman and Schmitz2006; Kaljo et al. Reference Kaljo, Hints, Männik and Nõlvak2008) started in the late mid-Katian (Bourahrouh, Paris & Elaouad-Debbaj, Reference Bourahrouh, Paris and Elaouad-Debbaj2004; Loi et al. Reference Loi, Ghienne, Dabard, Paris, Botquelen, Christ, Elaouad-Debbaj, Gorini, Vidal and Videt2010). During the deglaciation of the Hirnantian ice sheet, most Ordovician genera and species became extinct. A few Ordovician genera (e.g. Acanthochitina, Armoricochitina) disappeared during the deglaciation of the Hirnantian ice sheet, when about 33 % of the chitinozoan genera became extinct during the Late Ordovician. Almost all the species that originated in the Ordovician became extinct during the last part of the Hirnantian. The first chitinozoans with Silurian affinity (Spinachitina oulebsiri) occurred in the latest Hirnantian (upper Normalograptus persculptus Zone). Continuous sedimentation across the Ordovician/Silurian boundary is rare, but known from Skåne, south Sweden (Grahn, Reference Grahn1978, Reference Grahn1998; Nõlvak & Grahn, Reference Nõlvak and Grahn1993; Grahn & Nõlvak, Reference Grahn and Nõlvak2007b), possibly Anticosti Island, Canada (Achab, Reference Achab and Lespérance1981; Soufiane & Achab, Reference Soufiane and Achab2000; Bergström, Saltzman & Schmitz, Reference Bergström, Saltzman and Schmitz2006; Achab, Asselin & Desrochers, Reference Achab, Asselin, Desrochers, Kröger and Servais2008; Melchin, Reference Melchin2008) and Dob's Linn, Scotland (Verniers & Vandenbroucke, Reference Verniers and Vandenbroucke2006). In the former area, a barren zone occurs within the Normalograptus persculptus Zone, and before the appearance of Silurian chitinozoan lineages (e.g. Belonechitina postrobusta). At Dob's Linn the fossil record is not continuous. In Bohemia and southwestern France (A. Bourahrouh, unpub. Ph.D thesis, Univ. de Rennes, 2002), and Algeria (Paris, Bourahrouh & Le Hérissé, Reference Paris, Bourahrouh and le Hérissé2000; F. Paris, unpub. data), characteristic Ordovician species (e.g. Desmochitina minor, Armoricochitina nigerica, Calpichitina lenticularis, Tanuchitina elongata) thrived in open marine shelf environments after the end of the glaciation. They become extinct at the same level as in Skåne (that is, the uppermost Normalograptus persculptus Zone), but after the first occurrence of Silurian related taxa, such as Spinachitina oulebsiri-fragilis (Vandenbroucke et al. Reference Vandenbroucke, Gabbott, Paris, Aldridge and Theron2009b). The Hirnantian glaciation was therefore not directly responsible for the dramatic extinction of organic-walled microfossils. However, it certainly accelerated the extinction of lineages that had already been weakened since the Katian, and favoured development of taxa better adapted to the habitats available high in the water column above the anoxic sea-bottom environments that persisted in some northern Gondwana areas for 10–15 Ma (Paris, Bourahrouh & Le Hérissé, Reference Paris, Bourahrouh and le Hérissé2000; Le Hérissé et al. Reference Le Hérissé, Bourahrouh, Vecoli and Paris2003). Chitinozoans are abundant and highly diversified (Fig. 1) and recorded with other pelagic or epipelagic organisms such as graptolites, orthocones and leiospheres in the Silurian black shale. The poisoned anoxic sea-bottom was not suitable for any metazoan life (as indicated by lack of bioturbation, no benthic fossils, and no degradation of the organic matter). In western Gondwana the chitinozoophorans thrived during the early Silurian (Llandovery) deglaciations when the intracratonic basins had sea-way connections with the Rheic Ocean and subsequently shared the same fauna and phytoplankton (Grahn & Caputo, Reference Grahn and Caputo1992; Grahn, Reference Grahn2005; Villeneuve et al. Reference Villeneuve, Diallo, Keleba, Kourouma, Paris and Racheboeuf1989; S. De la Puente, unpub. Ph.D. thesis, Univ. Nacional de Córdoba, 2009).

5. The late Wenlock crisis (C. lundgreni event) and earliest Emsian (pre-basal Zlichov event) graptoloid extinction

At the end of the Wenlock, a regression (Johnson, Kaljo & Rong, Reference Johnson, Kaljo, Rong, Bassett, Lane and Edwards1991; Johnson & McKerrow, Reference Johnson and McKerrow1991; Kaljo & Märss, Reference Kaljo and Märss1991) severely affected the monograptids (C. lundgreni event) on a global basis (Koren & Urbanek, Reference Koren and Urbanek1994; Štorch, Reference Štorch1995; Kozlowska-Dawidziuk, Lenz & Štorch, Reference Kozlowska-Dawidziuk, Lenz and Štorch2001). Only Pristograptus dubius survived from the monograptid line. Although the chitinozoophorans shared part of the same niche as graptolites, they were less affected, but nevertheless the diversity decreased considerably (Figs 1, 2) in the late Wenlock–early Ludlow (Paris & Nõlvak, Reference Paris and Nõlvak1999; Paris et al. Reference Paris, Grahn, Nestor and Lakova1999). No glaciations or extraterrestrial (Jaeger, Reference Jaeger1991) events (as indicated by the lack of unusually high presence of iridium) are known from the end of the Wenlock that can explain the graptolite crisis on a global basis. Quinby-Hunt & Berry (Reference Quinby-Hunt and Berry1991) discussed a hydrochemical explanation. A high global temperature during the Silurian, and a low oxygen concentration in the atmosphere, probably led to an extensive oceanic anoxia (Quinby-Hunt & Berry, Reference Quinby-Hunt and Berry1991; Koren & Urbanek, Reference Koren and Urbanek1994). A possible scenario is, therefore, a change in reduction conditions in the oceans leading to anoxic waters at low depths, far from the bottom, and expanding into the graptolite habitat, which would lead to only a thin layer of pelagic waters suitable for life (Quinby-Hunt & Berry, Reference Quinby-Hunt and Berry1991; Koren & Urbanek, Reference Koren and Urbanek1994). The appearance of dolomites with interbedded graptolitic shales in the latest Wenlock corroborates the presence of anoxia in the oceans. Deep-sea dolomites occur only under an increased reducing potential of sediments. A global oceanic disturbance, as yet unidentified, which severely affected graptolites, should consequently be reflected in carbon isotope (δ13C) curves. These show depletion in some sections in the late Wenlock–early Ludlow (Corfield & Siveter, Reference Corfield and Siveter1992; Corfield et al. Reference Corfield, Siveter, Cartlidge and McKerrow1992; Kaljo, Kiipli & Martma, Reference Kaljo, Kiipli, Martma, Landing and Johnson1998). Chitinozoophorans were less affected (see Nestor, Reference Nestor2009) since they dominated in upper layers of the lower offshore to nearshore environments, while graptolites inhabited the pelagic (Vandenbroucke et al. Reference Vandenbroucke, Armstrong, Williams, Zalasiewicz and Sabbe2009a) or alternatively the deeper parts of the ocean (Cooper, Fortey & Lindholm, Reference Cooper, Fortey and Lindholm1991).

Graptoloid and chitinozoophoran diversity decreased dramatically during a regressive phase in the Pragian and earliest Emsian (Fig. 1), which resulted from the same oceanographic conditions as during the latest Wenlock (Jaeger, Reference Jaeger1991). In the Prague Basin the last graptoloids became extinct in the uppermost Dvorce-Prokop Limestone (Jaeger, Reference Jaeger1978), very close to base of the bursa chitinozoan biozone and to the former Pragian–Emsian transition (F. P., unpub. data). However, it must be stressed that this level is significantly younger than the controversial GSSP of the Emsian defined by the FAD of the Polygnathus kitabicus conodont index species (Yolkin et al. Reference Yolkin, Kim, Weddige, Talent and House2000). Only benthic dendroids survived the event (Chlupáč & Kukal, Reference Chlupáč and Kukal1988). During a transgressive phase in the early Emsian (basal Zlichov event), the chitinozoans were still abundant but fairly poorly diversified (e.g. Paris, Reference Paris1981). However, the disappearance of graptoloids had no major impact on the chitinozoan distribution, as new pelagic competitors occupied this more or less vacant pelagic niche after the disappearance of the graptoloids (e.g. ‘Thuringian ecotype’ ostracods; see Lethiers & Raymond, Reference Lethiers and Raymond1991).

6. Latest Frasnian anoxic crisis (Kellwasser event)

The latest Frasnian anoxic crisis (Kellwasser event) may be the consequence of a multiplicity of impacts (e.g. Alamo, Siljan, Flynn Creek). Moreover, these contributed to successive crises in the Frasnian (House, Reference House2002), and finally resulted in the latest Frasnian mass extinction (McGhee, Reference McGhee2001). Kellwasser sediments are characterized by a general decrease of detrital input, and an increasing burial of organic matter. There was a decrease in oceanic CO2 concentrations, that were very high during the Devonian, and an acceleration of terrestrial weathering (Elick, Driese & Mora, Reference Elick, Driese and Mora1998). The increasing bioproductivity and eutrophication of the epiric seas (Joachimski et al. Reference Joachimski, Pancost, Freeman, Ostertag-Henning and Buggisch2002; Filipiak, Reference Filipiak2002; Racki et al. Reference Racki, Racka, Matyja and Devleeschouwer2002) caused a decrease of oxygen levels and the development of anoxic sea-bottom conditions. Major tectonic movements (Racki, Reference Racki1998) in the late Frasnian are reflected in a higher hydrothermal volcanic influence (Pujol, Berner & Stüben, Reference Pujol, Berner and Stüben2006). A transgressive phase in the end of the Frasnian (Kellwasser event) occurred during a warm climate (Streel et al. Reference Streel, Caputo, Loboziak and Melo2000 and references therein). A regression in the beginning of the Famennian (Streel et al. Reference Streel, Caputo, Loboziak and Melo2000; House, Reference House2002) was caused by a cooler global climate (possibly a short-lived glaciation in the earliest Famennian). The exceptional high concentration of chitinozoans in the basal Famennian beds at La Serre, France, is probably not related to any physical mechanisms alone (Paris et al. Reference Paris, Girard, Feist and Winchester-Seeto1996). The Kellwasser event affected benthic fauna and probably also chitinozoan predators, and the chitinozoophorans could therefore expand in the cooler earliest Famennian environment. Despite the very high abundance of chitinozoans in the lowermost Famennian bed at La Serre, the assemblage is monospecific (Paris et al. Reference Paris, Girard, Feist and Winchester-Seeto1996). This drop of biodiversity was counterbalanced during the Famennian by a diversification of the group (Grahn & Melo, Reference Grahn and Melo2002) prior to the latest Famennian extinction. The peak in the 87Sr/86Sr curve (Burke et al. Reference Burke, Denison, Hetherington, Koepnick, Nelson and Otto1982; Veizer et al. Reference Veizer, Buhl, Diener, Ebeneth, Podlaha, Bruckschen, Jasper, Korte, Schaaf, Ala and Azmy1997) indicates an increase of silica in the oceans that might have been caused by the onset of the Eovariscan uplift and a mountain building-enhanced continental weathering (Averbuch et al. Reference Averbuch, Tribovillard, Devleeschouwer, Riquier, Mistiaen and van Vliet-Lanoe2005).

7. Extinction of the chitinozoophoran group

Despite numerous palynological investigations of early Carboniferous marine strata, no chitinozoans have been recorded in situ. However, Middle and Late Devonian chitinozoans are frequently found reworked into Tournaisian strata. Tasch & Hutter (Reference Tasch and Hutter1978) reported finding chitinozoans from the Carboniferous. However, these are reworked from the Devonian and we interpreted some of them (blistered structures) as cyanobacteria colonies. The last records of chitinozoans in situ are from Brazil (Grahn & Melo, Reference Grahn and Melo2002; Grahn, Loboziak & Melo, Reference Grahn, Loboziak and Melo2003) in the late Famennian prior to the latest Famennian glaciation (lower VH Zone = upper VCo Zone) and from the Retispora lepidophyta biozones in the Illizi Basin, Algeria (Abdesselam-Rouighi & Coquel, Reference Abdesselam-Rouighi and Coquel1997; Boumendjel et al. Reference Boumendjel, Loboziak, Paris, Steemans and Streel1988). In both areas, Fungochitina fenestrata is generally followed by a monospecific Fungochitina ultima assemblage (Paris et al. Reference Paris, Winchester-Seeto, Boumendjel and Grahn2000; Grahn & Melo, Reference Grahn and Melo2002; Grahn, Loboziak & Melo, Reference Grahn, Loboziak and Melo2003). The disappearance of the chitinozoans and therefore the extinction of the chitinozoophorans (Fig. 1) coincide with a regression and fall in sea-level (Hangenberg event) in connection with the glaciation in western Gondwana at the end of Famennian (lepidophyta biozones).

There are, however, several possible contributing factors to the extinction of the chitinozoophorans:

(1) The closing of oceans also disturbed the currents and thus the distribution of the food supply, as well as areas of upwelling. The assembly of Pangaea did not destroy the habitat of the chitinozoophorans as these planktic animals were in all Devonian oceans, including in the Panthalassa Ocean surrounding Pangaea. Moreover, suitable shallow marine environments were still available in the Early Carboniferous.

(2) The first forests developing in the early Famennian (Meyer-Berthaud, Scheckler & Wendt, 1999) drastically modified the terrigenous input in the ocean. The resulting chemical changes in the oceans and seas possibly affected the entire marine food chain, especially the phytoplankton.

(3) The development of these first significant forests led to an increase in the atmospheric oxygen level and possibly a decrease in the CO2 pressure. The influence of the latter on chitinozoan diversity may be better evaluated when well-documented δ13Corg curves are available and can be calibrated with chitinozoan biodiversity curves.

(4) The proliferation of more efficient predators in the pelagic niche, such as ‘Thuringian ecotype’ ostracods (see Lethiers & Raymond, 1991, fig. 6), generated a drastic increase in competition with the chitinozoophorans for the use of the food supply. Moreover, some components of this microfauna were potential chitinozoan consumers and thus affected the number of vesicles reaching the sea-bottom. The arrival of new competitors happened earlier with the development of the ostracods of ‘Thuringian ecotype’ during the Frasnian (Lethiers, Baudin & Casier, Reference Lethiers, Baudin and Casier1998), and even earlier with the entomozoidea ostracods in the Silurian. Because no dramatic consequences are noted for the abundance and diversity of the pre-Famennian chitinozoans, the role of these predators in the extinction of the chitinozoans should not be overestimated.

(5) The drop in acritarch diversity and subsequently of the phytoplankton productivity during the Late Devonian has to be stressed (Riegel, Reference Riegel2008). This might represent an important factor in the survival of chitinozoophorans: that is, insufficient food supply and more efficient new competitors, such as pelagic ostracods.

(6) The latest Famennian glaciation generated a drop in the sea-level with drastic changes in marine environments: much shallower seas, uplift and even erosion of land, as demonstrated by the common reworking of Middle and Late Devonian palynomorphs into the Carboniferous. In western Gondwana the onset of the latest Famennian glaciation changed open marine conditions to brackish environments as indicated by the appearance of Protosalvinia (Niklas, Phillips & Carozzi, Reference Niklas, Phillips and Carozzi1976; Loboziak et al. Reference Loboziak, Melo, Quadros and Streel1997) that occur somewhat later than the last chitinozoans (Grahn & Melo, Reference Grahn and Melo2002). This suggests that the chitinozoophorans were holomarine and could not adapt to brackish water conditions.

The chitinozoophorans became extinct for multiple and in some cases related reasons:

(1) They possibly no longer had the genetic potential to develop innovations favouring successful adaptations to rapid environmental changes (intrinsic factors). The monospecific assemblage in the latest Famennian supports this possibility.

(2) Their predators became more and more efficient (extrinsic factors). There are examples of selective predation from the late Llandovery in Saudi Arabia, documented by faecal pellets with cracked vesicles of a large species of Cyathochitina (F. P., unpub. data). Based on the size of the pellets, the predators were not very large and would have been part of the zooplankton (e.g. entomozoidea ostracods, including the Devonian ‘finger-print’ ostracods) or of the necto-pelagos (small polychaetes or arthropods such as crustaceans or crustacean larvae, but the poor preservation potential has left no body fossils recorded).

(3) Their usual niche was invaded by a more efficient group, such as pelagic ostracods (extrinsic factor), but this can be envisaged only if the competitor group had a dramatic increase in abundance in the Famennian (e.g. the ‘Thuringian ecotype’ ostracods; see Lethiers & Raymond, Reference Lethiers and Raymond1991, fig. 6). Indeed, other pelagic ostracods (pelagic entomozoidea and myodocope ostracods) are reported from the Wenlock onwards (see Siveter, Vannier & Palmer, Reference Siveter, Vannier and Palmer1991); V. J. Perrier, unpub. Ph.D. thesis, Univ. Claude Bernard, Lyon, 2007; Perrier, Vannier & Siveter, Reference Perrier, Vannier and Siveter2007) and they had no lethal effects on the chitinozoophorans.

(4) Their usual food supply disappeared or was not sufficient to share with more efficient feeding groups. This is supported by the contemporaneous decline in phytoplankton.

As a hypothesis, the chitinozoan record may promulgate a false idea of the situation if the chitinozoophorans had drastically changed their mode of life (e.g. become parasites) or their usual environment. For instance, the chitinozoophorans may have moved onto land, with an insect-type behaviour and a subsequent dramatic change in their eggs (see Paris, Reference Paris1981, p. 83). That is, there would no longer be any need to control osmotic pressure, but new membranes might have been necessary for the survival of the embryos. There are a number of similarities in ultrastructures between chitinozoans and modern insect eggs (Grahn & Afzelius, Reference Grahn and Afzelius1980; Paris, Reference Paris1981). Arthropods are known to have colonized land in the Silurian when the chitinozoophorans were thriving, for example, chelicerates in the early Llandovery (F. P., unpub. data) including myriapods (Morrissey & Braddy, Reference Morrissey and Braddy2004) and arachnids (Jeram, Selden & Edwards, Reference Jeram, Selden and Edwards1990) in the late Silurian. However, no significant diversification changes are noticed in the chitinozoan group at this time.

8. Concluding remarks

The chitinozoan group existed for about 130 Ma, from early Tremadocian to latest Famennian times. Chitinozoophorans (the chitinozoan animal) were pelagic zooplankton and shared part of this niche with graptolites and others. They were therefore less affected than other groups by the development of anoxic conditions in the deeper part of the water column (Rhuddanian black shales, Kellwasser event). Extinction of typical Ordovician taxa took place during the Hirnantian deglaciation, and while not directly responsible for the dramatic extinction of organic-walled microfossils, it certainly accelerated the extinction of lineages that had already been weakened since the Katian. This event also favoured the development of taxa better adapted to low oxygen levels in the anoxic oceanic environments prevalent during the Early Silurian (Rhuddanian). These Silurian lineages first appeared in the latest Hirnantian (upper Normalograptus persculptus Zone). Extinction of the chitinozoan group occurred after a combination of events that restricted the environments for the chitinozoophorans and favoured new competitors. This, combined with the fact that lineages had been weakened since the Frasnian and were monospecific in the latest Famennian, meant that they no longer had the genetic potential to develop innovations to adapt to successive environmental changes. The contemporaneous decline in phytoplankton indicates that the food supply disappeared or was insufficient for the chitinozoophorans. Together with the pressure of more predators, these factors contributed to their extinction.

Acknowledgements

Yngve Grahn thanks the Faculty of Geology at Universidade do Estado do Rio de Janeiro (UERJ), and Dr C. S. Valladares, head of the post-graduate progam at the Faculty of Geology for access to the facilities, and the Conselho Nacional de Desenvolvimento Cientifico e Tecnológico (CNPq, PQ 309751/2007-1) which made his work possible through grants. Oliver Chang Paris improved and updated the database (CHITINOVOSP) used by Florentin Paris for the evaluation of the chitinozoan biodiversity at species level. The authors are greatly indebted to Theresa Winchester-Seeto (Sydney, Australia) for scientific and linguistic improvements of the manuscript. We are indebded to Aicha Achab (Québec, Canada) for updated information on the range of the Late Ordovician chitinozoans in Laurentia. The reviewers, Thijs Vandenbroucke (Lille University, France) and Olle Hints (Tallinn Technical University, Estonia), are warmly acknowledged for helpful comments on the manuscript and for extensive discussions on the palaeooceanological distribution of the chitinozoans.

References

Abdesselam-Rouighi, F. F. & Coquel, R. 1997. Palynologie du Dévonien terminal–Carbonifère inférieur dans le Sud-Est du bassin d'Illizi (Sahara algérien). Position des premières lycospores dans la série stratigraphique. Annales de la Société Géologique du Nord T.5 (2eme sér.), 47–57.Google Scholar
Achab, A. 1981. Biostratigraphie par les Chitinozoaires de l'Ordovicien supérieur–Silurien inférieur de l'Ile d'Anticosti. Résultats préliminaires. In Subcommission on Silurian stratigraphy, Ordovician–Silurian Boundary Working Group (ed. Lespérance, P. J.), pp. 143–57. Field Meeting, Anticosti – Gaspé, Quebec, 1981. II. Stratigraphy and Paleontology.Google Scholar
Achab, A., Asselin, E. & Desrochers, A. 2008. Revisiting the Upper Ordovician chitinozoan assemblages from Anticosti Island: implications for local, regional and global correlation. In Paleozoic Climates (eds Kröger, B. & Servais, T.), p. 11. Abstracts, International Congress – Congrès international, August 22–31, 2008, Lille, France.Google Scholar
Achab, A. & Paris, F. 2007. The Ordovician chitinozoan biodiversification and its leading factors. Palaeogeography Palaeoclimatology Palaeoecology 245, 5–19.CrossRefGoogle Scholar
Ainsaar, L., Kaljo, D., Martma, T., Meidla, T., Männik, P., Nõlvak, J. & Tinn, O. 2010. Middle and Upper Ordovician carbon isotope chemostratigraphy in Baltoscandia: a correlation standard and clues to environmental history. Palaeogeography, Palaeoclimatology, Palaeoecology, 13 pp. Doi:10.1016/j;palaeo.2010.01.003.Google Scholar
Ainsaar, L., Meidla, T. & Martna, T. 2004. The Middle Caradoc facies and faunal turnover in the Late Ordovician Baltoscandian paleobasin. Palaeogeography Palaeoclimatology Palaeoecology 210, 119–33.CrossRefGoogle Scholar
Averbuch, O., Tribovillard, N., Devleeschouwer, X., Riquier, L., Mistiaen, B. & van Vliet-Lanoe, B. 2005. Mountain building-enhanced continental weathering and organic carbon burial as major causes for climatic cooling at the Frasnian–Fammenian boundary (c. 376 Ma)? Terra Nova 17, 25–34.CrossRefGoogle Scholar
Bergström, S. M., Chen, X., Gutiérrez-Marco, J. C. & Dronov, A. 2009 a. The new chronostratigraphic classification of the Ordovician System and its relations to major regional series and stages and to δ13C chemostratigraphy. Lethaia 42, 97–107.CrossRefGoogle Scholar
Bergström, S. M., Chen, X., Schmitz, B., Young, S., Rong, J. Y. & Saltzman, M. R. 2009 b. First documentation of the Ordovician Guttenberg δ13C excursion (GICE) in Asia: chemostratigraphy of the Pagoda and Yanwashan formations in southeastern China. Geological Magazine 146, 657–78.CrossRefGoogle Scholar
Bergström, S. M., Saltzman, M. M. & Schmitz, B. 2006. First record of the Hirnantian (Upper Ordovician) δ13C excursion in the North American Midcontinent and its regional implications. Geological Magazine 143, 657–78.CrossRefGoogle Scholar
Bloeser, B., Scopf, J. W., Hordystir, R. J. & Breed, W. J. 1977. Chitinozoans from the Late Precambrian Chuar group of the Grand Canyon, Arizona. Science 195, 676–9.CrossRefGoogle ScholarPubMed
Boumendjel, K., Loboziak, S., Paris, F., Steemans, P. & Streel, M. 1988. Biostratigraphy des miospores et des chitinozoaires du Silurien supérieur et du Dévonien dans le Bassin d'Illizi (S.E. du Sahara algérien). Geobios 21, 329–57.CrossRefGoogle Scholar
Bourahrouh, A., Paris, F. & Elaouad-Debbaj, Z. 2004. Biostratigraphy, biodiversity and palaeoenvironments of the chitinozoans and associated palynomorphs from the Upper Ordovician of the Central Anti-Atlas, Morocco. Review of Palaeobotany and Palynology 130, 17–40.CrossRefGoogle Scholar
Brett, C. A. & Baird, G. C. 1986. Comparative taphonomy: a key to paleoenvironmental interpretation based on fossil preservation. Palaios 1, 207–27.CrossRefGoogle Scholar
Burke, W. H., Denison, R. E., Hetherington, E. A., Koepnick, R. B., Nelson, H. F. & Otto, J. B. 1982. Variation of seawater 87Sr/86Sr through Phanerozoic time. Geology 10, 516–9.2.0.CO;2>CrossRefGoogle Scholar
Chen, X. H., Paris, F. & Zhang, M. 2008. Chitinozoans from the Fenxiang Formation (Early Ordovician) of Yichang, Hubei Province, China. Acta Geologica Sinica 82, 287–94.Google Scholar
Chlupáč, I. & Kukal, Z. 1988. Possible global events and the stratigraphy of the Palaeozoic of the Barrandian (Cambrian – Middle Devonian, Czechoslovakia). Sbornik geologichych věd Geologie 43, 83–146.Google Scholar
Collinson, C. & Schwalb, H. 1955. North American Paleozoic Chitinozoa. Illinois State Geological Survey Report of Investigations 186, 33 pp.Google Scholar
Combaz, A. 1967. Un microbios du Trémadocien dans un sondage d'Hassi-Messaoud. Actes de la Société Linnéenne de Bordeaux 104, 1–26.Google Scholar
Cooper, R. A. 1999. Ecostratigraphy, zonation and global correlation of earliest Ordovician planktic graptolites. Lethaia 32, 1–16.CrossRefGoogle Scholar
Cooper, R. A., Fortey, R. A. & Lindholm, K. 1991. Latitudinal and depth zonation of Early Ordovician graptolites. Lethaia 24, 199–218.CrossRefGoogle Scholar
Corfield, R. M. & Siveter, D. J. 1992. Carbon isotope change as indicator of biomass flue and an aid of correlation during ludensis–nilssoni (Silurian) time. Proceedings of the Estonian Academy of Sciences Geology 41, 173–81.CrossRefGoogle Scholar
Corfield, R. M., Siveter, D. J., Cartlidge, J. E. & McKerrow, S. 1992. Carbon isotope excursion near the Wenlock–Ludlow (Silurian) boundary in the Anglo-Welsh area. Geology 20, 371–4.2.3.CO;2>CrossRefGoogle Scholar
Dabard, M. P., Loi, A. & Paris, F. 2007. Relationship between phosphogenesis and sequence architecture: sequence stratigraphy and biostratigraphy in the Middle Ordovician of the Armoricain Massif (NW France). Palaeogeography Palaeoclimatology Palaeoecology 248, 339–56.CrossRefGoogle Scholar
De la Puente, S. & Rubinstein, C. 2009. Late Tremadocian chitinozoans and acritarchs from northwestern Argentina (Western Gondwana). Review of Palaeobotany and Palynology 154, 65–78.CrossRefGoogle Scholar
Destombes, J., Holland, C. H. & Willefert, S. 1985. Lower Palaeozoic rocks of Morocco. In Lower Palaeozoic Rocks of the World. Vol. 4, Lower Palaeozoic Rocks of Northwest and West-Central Africa (ed. Holland, C. H.), pp. 91–336. Chichester: John Wiley and Sons.Google Scholar
Eisenack, A. 1931. Neue Mikrofossilien des baltischen Silurs. 1. Paläontologische Zeitung 13, 74–118.CrossRefGoogle Scholar
Eisenack, A. 1955. Neue Chitinozoen aus dem Silur des Baltikums und dem Devon der Eifel. Senckenbergiana Lethaea 36, 311–9.Google Scholar
Eisenack, A. 1968. Über Chitinozoen des baltischen Gebietes. Palaeontographica Abteilung A 131, 137–98.Google Scholar
Elaouad-Debbaj, Z. 1988. Acritarches et Chitinozoaires du Tremadoc de l'Anti-Atlas central (Maroc). Revue de Micropaléontologie 31, 85–128.Google Scholar
Elick, J. M., Driese, S. G. & Mora, C. I. 1998. Very large plant and root traces from the Early to Middle Devonian: implications for early terrestrial ecosystems and atmospheric p(CO2). Geology 26, 143–6.2.3.CO;2>CrossRefGoogle Scholar
Filipiak, P. 2002. Palynofacies around the Frasnian/Famennian boundary in the Holy Cross Mountains, southern Poland. Palaeogeography Palaeoclimatology Palaeoecology 181, 313–24.CrossRefGoogle Scholar
Grahn, Y. 1978. Chitinozoan stratigraphy and palaeoecology of the Ordovician–Silurian boundary in Skåne, southern Sweden. Sveriges Geologiska Undersökning Serie C 766, 1–16.Google Scholar
Grahn, Y. 1981. Ordovician Chitinozoa from the Stora Åsbotorp boring in Västergötland, south-central Sweden. Sveriges Geologiska Undersökning Serie C 787, 1–40.Google Scholar
Grahn, Y. 1984 a. Ordovician Chitinozoa from Tallinn, northern Estonia. Review of Palaeobotany and Palynology 43, 5–31.CrossRefGoogle Scholar
Grahn, Y. 1984 b. Early Caradoc Chitinozoa from Östergötland, south central Sweden. Geologiska Föreningen i Stockholm Förhandlingar 105, 269–72.CrossRefGoogle Scholar
Grahn, Y. 1998. Lower Silurian (Llandovery–middle Wenlock) Chitinozoa and biostratigraphy of the mainland of Sweden. GFF 120, 273–83.CrossRefGoogle Scholar
Grahn, Y. 2005. Silurian and Lower Devonian chitinozoan taxonomy and biostratigraphy of the Trombetas Group, Amazonas Basin, Northern Brazil. Bulletin of Geosciences 80, 245–76.Google Scholar
Grahn, Y. & Afzelius, B. A. 1980. Ultrastructural studies of some chitinozoan vesicles. Lethaia 13, 119–26.CrossRefGoogle Scholar
Grahn, Y. & Caputo, M. V. 1992. Early Silurian glaciations in Brazil. Palaeogeography Palaeoclimatology Palaeoecology 99, 9–15.CrossRefGoogle Scholar
Grahn, Y., Loboziak, S. & Melo, J. H. G. 2003. Integrated correlation of Late Silurian (Pridoli s.l.) – Devonian chitinozoans and miospores in the Solimões Basin, northern Brazil. Acta Geologica Polonica 53, 283–300.Google Scholar
Grahn, Y. & Melo, J. H. G. 2002. Chitinozoan biostratigraphy of the Late Devonian formations in well Caima PH-2, Tapajós River area, Amazonas Basin, northern Brazil. Review of Palaeobotany and Palynology 118, 116–40.CrossRefGoogle Scholar
Grahn, Y. & Nõlvak, J. 2007 a. Remarks on older Ordovician Chitinozoa and biostratigraphy of the Oslo Region, southern Norway. GFF 129, 101–6.CrossRefGoogle Scholar
Grahn, Y. & Nõlvak, J. 2007 b. Ordovician Chitinozoa and biostratigraphy from Skåne and Bornholm, southernmost Scandinavia – an overview and update. Bulletin of Geosciences 82, 11–26.CrossRefGoogle Scholar
Grahn, Y. & Nõlvak, J. 2010. Swedish Ordovician Chitinozoa and biostratigraphy: a review and new data. Palaeontographica Abteilung B 283 (1–3), 1–67.Google Scholar
Hamoumi, N. 1999. Upper Ordovician glaciation spreading and its sedimentary record in Moroccan North Gondwana margin. Acta Universitatis Carolinae, Geologica 43, 111–14.Google Scholar
Heuse, T., Grahn, Y. & Erdtmann, B.-D. 1999. Early Ordovician chitinozoans from the east Precordillera of southern Bolivia. Revue de Micropaléontologie 42, 43–55.CrossRefGoogle Scholar
Hints, O., Delabroye, A., Nõlvak, J., Servais, T., Uutela, A. & Wallin, Å. 2010. Biodiversity patterns of Ordovician marine phytoplankton from Baltica: comparison with other fossil groups and sea-level changes. Palaeogeography Palaeoclimatology Palaeoecology, 13 pp. Doi:10.1016/j;palaeo.2009.11.003.Google Scholar
Hints, O. & Nõlvak, J. 2006. Early Ordovician scolecodonts and chitinozoans from Tallinn, north Estonia. Review of Palaeobotany and Palynology 139, 189–209.CrossRefGoogle Scholar
House, M. R. 2002. Strength, timing and cause of mid-Palaeozoic extinctions. Palaeogeography Palaeoclimatology Palaeoecology 181, 5–25.CrossRefGoogle Scholar
Jacob, J., Paris, F., Monod, O., Miller, M. A., Tang, P., George, S. C. & Bény, J.-M. 2007. New insights into the chemical composition of the chitinozoans. Organic Geochemistry 38, 1782–8.CrossRefGoogle Scholar
Jaeger, H. 1978. Late graptoloid faunas and the problem of graptoloid extinction. Acta Palaeontologica Polonica 23, 497–521.Google Scholar
Jaeger, H. 1991. Neue Standard-Graptolithenzonenfolge nach der “Grosen Krise” an der Wenlock/Ludlow-Grenze (Silur). Neues Jahrbuch für Geologie und Paläontologie Abhandlungen 182, 303–54.CrossRefGoogle Scholar
Jenkins, W. A. M. 1970. Chitinozoa. Geoscience and Man 1, 21 pp.CrossRefGoogle Scholar
Jeram, A. J., Selden, P. A. & Edwards, D. 1990. Land animals in the Silurian: arachnids and myriapods from Shropshire, England. Science 250, 658–61.CrossRefGoogle ScholarPubMed
Joachimski, M. M., Pancost, R. D., Freeman, K. H., Ostertag-Henning, C. & Buggisch, W. 2002. Carbon isotope geochemistry of the Frasnian–Famennian transition. Palaeogeography Palaeoclimatology Palaeoecology 181, 91–109.CrossRefGoogle Scholar
Johnson, M. E., Kaljo, D. L. & Rong, J. Y. 1991. Silurian eustasy. In The Murchison Symposium: Proceedings of an International Conference on the Silurian System (eds Bassett, M. G., Lane, P. D. & Edwards, D.), pp. 145–63. Special Papers in Palaeontology 44.Google Scholar
Johnson, M. E. & McKerrow, W. S. 1991. Sea level and faunal changes during the latest Llandovery and earliest Ludlow (Silurian). Historical Biology 5, 153–69.CrossRefGoogle Scholar
Kaljo, D. L., Hints, L., Männik, P. & Nõlvak, J. 2008. The succession of Hirnantian events based on data from Baltica: brachiopods, chitinozoans, conodonts, and carbon isotopes. Estonian Journal of Earth Sciences 57, 197–218.CrossRefGoogle Scholar
Kaljo, D. L., Kiipli, T. & Martma, T. 1998. Correlation of carbon isotope events and environmental cyclicity in the East Baltic Silurian. In Silurian Cycles – Linkages of Dynamic Stratigraphy with Atmospheric, Oceanic and Tectonic Changes (eds Landing, E. & Johnson, M.), pp. 297–312. New York State Museum Bulletin no. 491.Google Scholar
Kaljo, D. L. & Märss, T. 1991. Pattern of some Silurian bioevents. Historical Biology 5, 145–52.CrossRefGoogle Scholar
Koren, T. N. & Urbanek, A. 1994. Adaptive radiation of monograptids after the late Wenlock crisis. Acta Geologica Polonica 39, 137–67.Google Scholar
Kozlowska-Dawidziuk, A., Lenz, A. C. & Štorch, P. 2001. Upper Wenlock and Lower Ludlow (Silurian) post-extinction graptolites, Všeradice Section, Barrandian area, Czech Republic. Journal of Paleontology 75, 147–64.2.0.CO;2>CrossRefGoogle Scholar
Kozlowski, R. 1963. Sur la nature des Chitinozoaires. Acta Paleontologica Polonica 8, 425–49.Google Scholar
Le Hérissé, A., Bourahrouh, A., Vecoli, M. & Paris, F. 2003. Palynological tracers of sea-ice cover extent during the latest Ordovician on the North African margin. AAPG Hedberg conference. Paleozoic and Triassic petroleum systems in North Africa, February 18–20, Algiers, Algeria, pp. 1–2.Google Scholar
Lehnert, O., Männik, P., Joachimski, M. M., Calner, M. & Fryda, J. 2010. Palaeoclimate perturbations before the Sheinwoodian glaciation: a trigger for extinctions during the “Ireviken Event”. Palaeogeography Palaeoclimatology Palaeoecology, 12 pp. Doi:10.1016/j.palaeo.2010.01.009.Google Scholar
Lethiers, F., Baudin, F. & Casier, J. G. 1998. Ostracodes de la limite Frasnien–Famennien en environment anoxique (La Serre, Montagne Noire, France). Revue de Micropaléontologie 41, 321–36.CrossRefGoogle Scholar
Lethiers, F. & Raymond, D. 1991. Les crises du Dévonien supérieur par l’étude des faunes d'ostracodes dans leur cadre paléogéographique. Palaeogeography Palaeoclimatology Palaeolecology 88, 133–46.CrossRefGoogle Scholar
Loboziak, S., Melo, J. H. G., Quadros, L. P. & Streel, M. 1997. Palynological evaluation of the Famennian Protosalvinia (Foerstia) Zone in the Amazonas Basin, northern Brazil: a preliminary study. Review of Palaeobotany and Palynology 96, 31–45.CrossRefGoogle Scholar
Loi, A., Ghienne, J. F., Dabard, M. P., Paris, F., Botquelen, A., Christ, N., Elaouad-Debbaj, Z., Gorini, A., Vidal, M. & Videt, B. 2010. The Late Ordovician glacio-eustatic record from a high-latitude storm-dominated shelf succession: the Bou Ingarf section (Anti-Atlas, Southern Morocco). Palaeogeography, Palaeoclimatology, Palaeoecology, 27 pp. Doi: 10.1016/j.palaeo.2010.01.018.Google Scholar
McGhee, G. R. 2001. The “multiple impacts hypothesis” for mass extinction: a comparison of the Late Devonian and the late Eocene. Palaeogeography Palaeoclimatology Palaeoecology 176, 47–58.CrossRefGoogle Scholar
Melchin, M. J. 2008. Restudy of some Ordovician–Silurian boundary graptolites from Anticosti Island, Canada, and their biostratigraphic significance. Lethaia 41, 155–62.CrossRefGoogle Scholar
Meyer-Berthaud, B., Scheckler, S. E. & Wendt, J. 1999. Archaeopteris is the earliest known modern tree. Nature 398, 700–1.CrossRefGoogle Scholar
Morrissey, L. B. & Braddy, S. J. 2004. Terrestrial trace fossils from the Lower Old Red Sandstone, southwest Wales. Geological Journal 39, 315–36.CrossRefGoogle Scholar
Nestor, V. 2009. Chitinozoan diversity in the East Baltic Silurian. Estonian Journal of Earth Sciences 58, 311–6.CrossRefGoogle Scholar
Niklas, K. J., Phillips, T. L. & Carozzi, A. V. 1976. Morphology and paleoecology of Protosalvinia from the Upper Devonian (Famennian) of the Middle Amazon Basin of Brazil. Palaeontographica Abteilung B 155, 1–30.Google Scholar
Nõlvak, J. 1999. Ordovician chitinozoan biozonation of Baltoscandia. Acta Universitatis Carolinae, Geologica 43, 287–90.Google Scholar
Nõlvak, J. & Grahn, Y. 1993. Ordovician chitinozoan zones from Baltoscandia. Review of Palaeobotany and Palynology 79, 245–69.CrossRefGoogle Scholar
Ogg, J. G., Ogg, G. & Gradstein, F. M. 2008. Concise Geologic Time Scale. Cambridge University Press, 177 pp.Google Scholar
Paris, F. 1981. Les Chitinozoaires dans le Paléozoïque du sud-ouest de l'Europe (cadre géologique – étude systématique – biostratigraphie). Mémoire de la Société géologique et minéralogique de Bretagne 26, 492 pp.Google Scholar
Paris, F. 1984. Bassins paléozoïques caches d'Aquitaine; biostratigraphie par les Chitinozoaires, Ostracodes, Tentaculites. Documents de BRGM, 13–17.Google Scholar
Paris, F. 1990. The Ordovician chitinozoan biozones of the Northern Gondwana Domain. Review of Palaeobotany and Palynology 66, 181–209.CrossRefGoogle Scholar
Paris, F., Achab, A., Asselin, E., Chen, X.-H., Grahn, Y., Nõlvak, J., Obut, O., Sennikov, N., Vecoli, M., Verniers, J., Wang, X.-F. & Winchester-Seeto, T. 2004. Chapter 28: Chitinozoans. In The Great Ordovician Biodiversification Event (eds Webby, B. D., Paris, F., Droser, M. L. & Percival, I. G.), pp. 294–311. New York: Columbia University Press.CrossRefGoogle Scholar
Paris, F. & Bernard, D. 1994. “PHOTOCHITINO”, an image-incorporated electronic database for chitinozoan identification. In CIMP Symposium on Palynology, Palaeoenvironments and Stratigraphy (eds Dorning, K. et al. ), p. 32. Abstract. Sheffield, 7–10 September 1994.Google Scholar
Paris, F., Bourahrouh, A. & le Hérissé, A. 2000. The effects of the final stages of the Late Ordovician glaciation on marine palynomorphs (chitinozoans, acritarchs, leiospheres) in well NI-2 (NE Algerian Sahara). Review of Palaeobotany and Palynology 113, 87–104.CrossRefGoogle Scholar
Paris, F., Girard, C., Feist, C. & Winchester-Seeto, T. 1996. Chitinozoan bio-event in the Frasnian/Famennian boundary beds at La Serre (Montagne Noire, Southern France). Palaeogeography Palaeoclimatology Palaeoecology 121, 131–45.CrossRefGoogle Scholar
Paris, F., Grahn, Y., Nestor, V. & Lakova, I. 1999. Proposal for a revised chitinozoan classification. Journal of Paleontology 73, 549–70.CrossRefGoogle Scholar
Paris, F. & Nõlvak, J. 1999. Biological interpretation and paleobiodiversity of a cryptic fossil group: the “Chitinozoan animal”. Geobios 32, 315–24.CrossRefGoogle Scholar
Paris, F., Winchester-Seeto, T., Boumendjel, K. & Grahn, Y. 2000. Toward a global biozonation of Devonian chitinozoans. Courier Forschungsinstitut Senckenberg 220, 39–55.Google Scholar
Perrier, V. J., Vannier, D. J. & Siveter, D. J. 2007. The Silurian pelagic myodocope ostracode Richteria migrans. Earth and Environmental Science Transactions of the Royal Society of Edinburgh 98, 151–63.CrossRefGoogle Scholar
Porter, S. M. & Knoll, A. H. 2000. Testate amoebae in the Neoproterozoic Era: evidence from vase-shaped microfossils in the Chuar group, Grand Canyon. Paleobiology 26, 360–85.2.0.CO;2>CrossRefGoogle Scholar
Porter, S. M., Meisterfeld, R. & Knoll, A. H. 2003. Vase-shaped microfossils from the Neoproterozoic Chuar Group, Grand Canyon: a classification guided by modern testate amoebae. Journal of Paleontology 77, 409–29.2.0.CO;2>CrossRefGoogle Scholar
Poumot, C. 1964. Trois nouveaux genres de Chitinozoaires de l'Ordovicien. Documents internes CIMP(1965), 62–75.Google Scholar
Poumot, C. 1968. Amphorachitina, Ollachitina, Velatachitina, Trois nouveaux Genres de Chitinozoaires de l'Erg Oriental (Algérie-Tunisie). Bulletin centre de recherches. Elf exploration production, Pau 2, 45–55.Google Scholar
Pujol, F., Berner, Z. & Stüben, D. 2006. Palaeoenvironmental changes at the Frasnian/Famennian boundary in key European sections: chemostratigraphic constraints. Palaeogeography Palaeoclimatology Palaeoecology 240, 120–45.CrossRefGoogle Scholar
Quinby-Hunt, M. S. & Berry, W. B. N. 1991. Late Wenlock (Middle Silurian) Global bioevent: possible chemical cause for mass graptolite mortalities. Historical Biology 5, 171–81.CrossRefGoogle Scholar
Racki, G. 1998. Frasnian–Famennian biotic crisis: undervaluated tectonic control? Palaeogeography Palaeoclimatology Palaeoecology 141, 177–98.CrossRefGoogle Scholar
Racki, G., Racka, M., Matyja, H. & Devleeschouwer, X. 2002. The Frasnian/Famennian boundary interval in the South Polish–Moravian shelf basins: integrated event–stratigraphical approach. Palaeogeography Palaeoclimatology Palaeoecology 181, 251–97.CrossRefGoogle Scholar
Riegel, W. 2008. The Late Palaeozoic phytoplankton blackout – artefact or evidence of global change? Review of Palaeobotany and Palynology 148, 73–90.CrossRefGoogle Scholar
Sadler, P. M., Cooper, R. A. & Melchin, M. 2009. High-resolution, early Paleozoic (Ordovician–Silurian) time scales. Geological Society of America Bulletin 121, 887–906.CrossRefGoogle Scholar
Samuelsson, J. 1999. Ordovician Chitinozoa from Rügen, North-East Germany. In Quo Vadis Ordovician? 8th International Symposium on Ordovician System, Prague (eds Kraft, P. & Fatka, O.), pp. 295–7. Acta Universitatis Carolinae, Geologica 43.Google Scholar
Sennikov, N. V., Yolkin, E. A., Petrunina, Z. E., Gladkikh, L. A., Obut, O. T., Izokh, N. G. & Kipriyanova, T. P. 2008. Ordovician–Silurian biostratigraphy and paleogeography of the Gorny Altai. In Trofimuk Institute of Petroleum Geology and Geophysics Sb Ras (eds Sennikov, A. V. & Kanygin, A. V.), pp. 1–156. Novosibirsk; Publishing House Sb Ras.Google Scholar
Servais, T., Lehnert, O., Li, J., Mullins, G. L., Munnecke, A., Nützel, A. & Vecoli, M. 2008. The Ordovician biodiversification: revolution in the oceanic trophic chain. Lethaia 41, 99–109.CrossRefGoogle Scholar
Siveter, D. J., Vannier, D. J. & Palmer, M. C. 1991. Silurian myodocopes: pioneer pelagic ostracodes and the chronology of an ecological shift. Journal of Micropalaeontology 10, 151–73.CrossRefGoogle Scholar
Soufiane, A. & Achab, A. 2000. Chitinozoan zonation of the Late Ordovician and the Early Silurian of the island of Anticosti, Québec, Canada. Review of Palaeobotany and Palynology 109, 85–111.CrossRefGoogle ScholarPubMed
Stanley, G. D. Jr & Sturmer, W. 1983. The first fossil ctenophore from the Lower Devonian of West Germany. Nature 303, 518–20.CrossRefGoogle Scholar
Štorch, P. 1995. Biotic crisis and post-crisis recoveries recorded by Silurian planktonic graptolite faunas of the Barrandian area (Czech Republic). Geolines (Praha) 3, 59–70.Google Scholar
Streel, M., Caputo, M. V., Loboziak, S. & Melo, J. H. G. 2000. Late Frasnian–Famennian climates based on palynomorph analyses and the question of the Late Devonian glaciations. Earth Science Reviews 52, 121–73.CrossRefGoogle Scholar
Tasch, P. & Hutter, T. J. 1978. Pennsylvanian chitinozoans from Eastern Kansas. Palinologia, núm. extraord. 1, 443–52.Google Scholar
Trotter, J. A., Williams, I. S., Barns, C. R., Lécuyer, C. & Nicoll, R. S. 2008. Did cooling oceans trigger Ordovician biodiversification? Evidence from conodont thermometry. Science 321, 550–4.CrossRefGoogle ScholarPubMed
Vandenbroucke, T., Armstrong, H. A., Williams, M., Paris, F., Sabbe, K., Zalasiewicz, J. A. & Nõlvak, J. 2010. Epipelagic chitinozoan biotopes map a steep latitudinal temperature gradient for earliest Late Ordovician seas: implications for a cooling Late Ordovician climate. Palaeogeography Palaeoclimatology Palaeoecology, 18 pp. Doi: 10.1016/j.palaeo.2009.11.026.Google Scholar
Vandenbroucke, T., Armstrong, H. A., Williams, M., Zalasiewicz, J. A. & Sabbe, K. 2009 a. Ground-truthing Late Ordovician climate models using the paleobiogeography of graptolites. Paleoceanography 24, PA 4202.CrossRefGoogle Scholar
Vandenbroucke, T., Gabbott, S. E., Paris, F., Aldridge, R. J. & Theron, J. N. 2009 b. Chitinozoans and the age of the Soom Shale, an Ordovician black shale Lagerstätte, South Africa. Journal of Micropalaeontology 28, 53–66.CrossRefGoogle Scholar
Veizer, J., Buhl, D., Diener, A., Ebeneth, S., Podlaha, O. G., Bruckschen, P., Jasper, T., Korte, C., Schaaf, M., Ala, D. & Azmy, K. 1997. Strontium isotope stratigraphy: potential resolution and event correlation. Palaeogeography Palaeoclimatology Palaeoecology 132, 65–77.CrossRefGoogle Scholar
Verniers, J. & Vandenbroucke, T. 2006. Chitinozoan biostratigraphy in the Dob's Linn Ordovician–Silurian GSSP, Southern Uplands, Scotland. GFF 128, 195–202.CrossRefGoogle Scholar
Videt, B., Paris, F., Rubino, J.-L., Boumendjel, K., Dabard, M.-P., Loi, A. & Ghienne, J.-F. 2010. Calibration of Ordovician sequences on the northern Gondwana platform. Palaeogeography Palaeoclimatology Palaeoecology, Doi: 10.1016/j.palaeo.2010.03.050, in press.CrossRefGoogle Scholar
Villeneuve, M., Diallo, M. C., Keleba, F., Kourouma, S., Paris, F. & Racheboeuf, P. R. 1989. Données paléontologiques nouvelles sur le Paléozoïque du Bassin Bové (Guinée, Afrique de l'Ouest): conséquences stratigraphiques. Comptes rendus de l'Académie des Sciences de Paris 309, 1583–90.Google Scholar
Voss-Foucart, M. F. & Jeuniaux, C. 1972. Lack of chitin in a sample of Ordovician Chitinozoa. Journal of Paleontology 46, 769–70.Google Scholar
Williams, S. H., Nowlan, G. S., Barnes, C. R. & Batten, R. S. R. 1999. The Ledge section at Cow Head, western Newfoundland: new data and discussion of the graptolite, conodont and chitinozoan assemblages. Acta Universitatis Carolinae, Geologica 43, 65–8.Google Scholar
Yolkin, E. A., Kim, A. I., Weddige, K., Talent, J. A. & House, M. R. 2000. The basal Emsian GSSP in Zinzil'ban Gorge, Uzbekistan. Courier Forschungsinstitut Senckenberg 225, 17–25.Google Scholar
Zhu, M.-Y., Badcock, L. E. & Peng, S.-C. 2006. Advances in Cambrian stratigraphy and paleontology: integrating correlation techniques, paleobiology, taphonomy and paleoenvironmental reconstruction. Palaeoworld 15, 217–22.CrossRefGoogle Scholar
Figure 0

Figure 1. Global evaluation of the chitinozoan biodiversification from the origin of the group in the early Tremadocian to its extinction in the latest Devonian. The solid circles indicate the number of species per stage (Ordovician and Devonian) or per series (Silurian). The graph represents the mean diversity of the chitinozoans per million years for the stages or series (durations based on Sadler, Cooper & Melchin, 2009). An alternative graph (dashed line) is based on the time calibration by Ogg, Ogg & Gradstein (2008). The most significant events are indicated along the time scale. Open arrow: Darriwilian cooling (Trotter et al. 2008; Ainsaar et al. 2010); black arrow: biological and oceanological events (Jaeger, 1978, 1991; Meyer-Berthaud, Scheckler & Wendt, 1999; House, 2002; Joachimski et al. 2002; Kaljo et al. 2008; Servais et al. 2008; Bergström et al. 2009a; Hints et al. 2010); black star: main anoxic events (Chlupáč & Kukal, 1988; House, 2002); circled star: main glacial events (Streel et al. 2000; Lehnert et al. 2010). The values of the biodiversity of the chitinozoan at species level are from the database ‘CHITINOVOSP’ of F. Paris.

Figure 1

Figure 2. Global biodiversity of the Silurian chitinozoans species per stage (solid circles) and mean value of their specific diversity per million years for each stage. (Numerical calibration from Sadler, Cooper & Melchin, 2009.)