Conodont dating of some Telychian (Silurian) sections in Estonia/Telychiani (Silur) paljandite vanusest Eestis konodontide leviku pohjal.

INTRODUCTION

Different intervals of Telychian (Adavere Stage) and/or lower Sheinwoodian (Jaani Stage) strata are exposed in the sections discussed below. The intervals are dominated by various marlstones which, according to Nestor & Einasto (1997), formed during a transgressive (deepening) phase of the late Llandovery-middle Wenlock macrocycle of basin development. Three units, the Rumba and Velise formations in the Adavere Stage, and the Mustjala Member of the Jaani Formation in the lower part of the Jaani Stage, span this interval in the outcrop area. In terms of sequence stratigraphy, the strata of the Adavere Stage correspond to Sequence 4 (S4) and those of the Mustjala Member to the lower part of Sequence 5 (S5) (Harris et al. 2005). A major flooding event marks the base of S4. This sequence is separated from the underlying sequence S3, which corresponds to the upper half of the Raikkula Stage, by an extensive gap in the region. At this level a gap has been recognized globally, e.g. in Australia, where it is known as the Panuara Hiatus (Bischoff 1986). The boundary between S4 and SS is marked by submarine erosion (or slumping) on the buried palaeoslope and local (along the western coast of modern Estonia) deposits of redeposited ooids. To the east of the belt with ooids a distinct gap occurs at the sequence boundary, increasing in duration to the northeast.

The Rumba Formation is represented by a cyclic succession of marlstones to argillaceous limestones and relatively pure limestones (Einasto et al. 1972). A very rich association of shallow-water benthic fossils occurs in these strata, sometimes as scattered valves, sometimes as clusters of complete shells in living position, and sometimes as tempestitic accumulations of Pentamerus oblongos Sowerby (Kaljo 1970). The overlying Velise Formation and the succeeding Mustjala Member of the Jaani Formation are lithologically very similar. These units consist of different marlstones and madstones (plastic clays in the lower part of the succession) and are difficult to separate in continuous sections where lithological changes are gradual (e.g. in the Viki core of western Saaremaa; Nestor 1990). However, it has been argued that in the mainland part of Estonia the strata of the Mustjala Member are much more dolomitized than marlstones of the Velise Formation (Aaloe 1970; Nestor 1997) and these two units can be separated on the basis of this feature. As the boundary between the Velise and Jaani formations has traditionally been considered to correspond to the boundary between the Adavere and Jaani stages (e.g. Nestor 1997), dolomitic marlstones in some sections (e.g. in Avaste; Aaloe 1970) have been dated as of Jaani (early Wenlock) age. However, it is evident now (see below) that this dating is not correct and that the strata exposed in the Avaste section are older.

Recent detailed studies of conodonts from Telychian and Sheinwoodian strata have enabled considerable improvement of conodont biostratigraphy for this interval (Jeppsson 1997; Mannik 2007a). On the basis of these data, it has become possible to date precisely the Telychian-lowermost Sheinwoodian strata exposed in many sections in western Central Estonia (Fig. 1). Below, several of these sections are characterized briefly and the conodont faunas are discussed.

[FIGURE 1 OMITTED]

All figured specimens of conodonts are deposited in collection GIT 555 in the Institute of Geology at Tallinn University of Technology, Estonia.

STUDIED SECTIONS

Seven sections (Valgu-1, Valgu-2, Valgu-3, Velise-Korgekalda, Jadivere, Avaste, and Saastna), located in west-central and western continental Estonia, were sampled for conodonts (Fig. 1). The average size of samples was 2-4 kg, but some samples from the Valgu-1 section (M-882, M-872, M-873, M-874, M-876), weighing more than 10 kg, were processed. All samples except for the lowermost one (M-1963) in the Valgu-1 section yield rich conodont faunas, allowing reliable location of the studied strata in the conodont zonal succession.

Sections in the Valgu region

Three sections, one at the drainage canal (Valgu-1) and two on the left bank of the Velise River (Valgu-2 and Valgu-3) were studied. All sections are located close to one another, about 0.8 km east-northeast of the main crossroad in Valgu village (Figs 1, 2).

The valgu-1 section

In this section the upper part of the Rumba Formation and the lowermost Velise Formation are exposed (Fig. 2). Lithologically the Rumba Formation (exposed mainly just north of the Valgu-Rapla road; Fig. 2B) is dominated by light-grey variously dolomitized argillaceous to bioclastic limestones with abundant shells of Pentamerus oblongus in many beds. Discontinuity surfaces are common. As a rule, the surfaces are smooth, with abundant up to 2 cm deep holes, and variously pyritized. Often the discontinuity surfaces cut the shells of Pentamerus oblongus. Occasional tabulate corals, stromatoporoids, and trilobites have been found (Klaamann 1984b).

Two samples were studied from the uppermost Rumba Formation (Fig. 2), both of which yielded conodonts. In the lower sample (M-1963; 0.05-0.15 m below the upper boundary of the Rumba Formation; weight 4.15 kg) only two conodont specimens, one identified as Panderodus cf. unicostatus (Branson & Mehl) and the other as Distomodus cf. staurognathoides (Walliser), were found. The next sample (M-1962; weight 5.31 kg) comes from a bed between two discontinuity surfaces, the upper of which is considered to correspond to the boundary between the Rumba and Velise formations. This sample contains rich conodont fauna, similar to that of the overlying Velise Formation (see below). The contact between the Rumba and Velise formations is exposed close to the road (on both sides). The base of the Velise Formation is represented by a bed (2-3 cm in thickness) of bioturbated argillaceous bioclastic limestone.

The Velise Formation is dominated by grey, bluish-grey, and greenish-grey argillaceous to calcareous, often bioturbated, marlstones, with rare thin interbeds of argillaceous limestone, sometimes rich in bioclastic material. Nodules of similar limestone are common in some intervals. Three bentonites have been found in the section. The lowermost one is up to 10-13 cm thick, of light yellowish colour and hard. The uppermost part of this bentonite is strongly bioturbated. The burrows are filled with greenish-grey calcareous marlstone. A thin (2-3 cm) interbed of calcareous clay divides the bentonite into two parts of almost equal thickness. Two additional bentonites, located higher in the section, are thin (1-3 cm), light-coloured (yellowish), and also hard. All three bentonites are also recognized in the Valgu-2 section and the upper two in the Valgu-3 section (see below; Fig. 3).

[FIGURE 2 OMITTED]

[FIGURE 3 OMITTED]

The samples from the Velise Formation contain rich and variable conodont faunas (Fig.2) characterized mainly by Pterospathodus eopennatus ssp. n. 1 Mannik, Aulacognathus kuehni Mostler, Apsidognathus milleri (Over & Chatterton), and, only in the lower part of the section, Astropentagnathus irregularis Mostler. Platform-bearing genera (Apsidognathus, Astropentagnathus, Aulacognathus, Distomodus) are important, with Apsidognathus being represented at least by two different species.

The Palgu-2 and Palgu-3 sections

Outcrops along the Velise River in Valgu village have been known for a long time (e.g. Rosenstein 1939; Jurgenson 1964, 1966). Now the cliffs, once well exposed along the river, are mostly covered and just a few parts of them are accessible for study. The two sections sampled for conodonts and to be discussed here are located on the left bank of the Velise River, about 1.0 and 1.2 km upstream from the bridge across the river on the Valgu-Libatse road (Fig. 2). In these sections the same strata (excluding the Rumba Formation) as in the Valgu-1 section are exposed. In the upper part of the Valgu-3 section strata younger than the uppermost beds studied in Valgu-1 are exposed. Lithologically, the succession of strata in these two sections is similar to that in the Valgu-1 section (Figs 2 and 3), although in Valgu-2 and Valgu-3 the rock is slightly dolomitized. Conodont faunas are similar in all three sections. In the Valgu-3 section only the strata above the uppermost bentonite were sampled for conodonts (Fig. 3).

The Velise-Korgekalda section

The section is located on the left bank of the Velise River, about 2.3 km from the bridge at Velise towards Paardu village, 0.2 km north of the road (Figs 1, 4). The outcrop, mostly covered by debris and vegetation, is a natural cliff up to 4-5 m high, and can be followed for more than 100 m along the river. The strata are better exposed at the downstream end of the cliff. Here, the section shown in this paper was described and sampled.

The lowermost strata accessible in the section consist of argillaceous bioclastic limestones with abundant pyrite aggregates of various sizes. This bed forms the floor of the river channel. An interbed of similar limestone, a few decimetres thick, occurs about a metre higher in the section. The section is dominated by argillaceous marlstones which contain abundant nodules of calcareous marlstone, and burrows up to 2.5-3 cm in diameter, filled with calcareous material rich in bioclasts. This interval, as a rule, is covered by debris and vegetation. The uppermost 1 m of the section is more calcareous and forms an almost vertical cliff. The upper contact of the Telychian strata is erosional and is followed by Quaternary glacial and limnoglacial deposits with a thickness of up to 2 m.

Most significant in the rich conodont faunas in the Velise-Korgekalda section is the occurrence of Pterospathodus amorphognathoides angulatus (Walliser) and Apsidognathus tuberculatus ssp. n. 3 (Fig. 4). The oldest known specimen of Nudibelodina sensitiva Jeppsson has been found in sample V1-2 from the base of this section.

The Jadivere section

The section is located on the left bank of the Enge River, west of the bridge (about 200 m downstream of it) on the Tallinn-Parnu road (Figs 1, 5). The section is up to 2.5 m high and nowadays almost completely covered by debris. However, as the layer of debris is thin, the bedrock is easy to clean out. Lithologically the section consists of monotonous light bluish-grey marlstones, more calcareous in the lower and argillaceous in the upper parts of the section. Benthic macrofossils appear to be entirely absent, although rare tiny fragments of unidentified organisms(?) occur sporadically. The age of the strata exposed in the Jadivere outcrop has been problematic. Originally, they were assigned to the Jaani Stage (Aaloe 1970). Later, P. amorphognathoides Walliser was indentified in the section, which dated the marlstones outcropping here to the corresponding zone at the Llandovery-Wenlock transition (Klaamann 1984a). Recent studies have revealed that P. amorphognathoides in this section is represented by P. a. lennarti Mannik, known only from strata of Telychian age (Mannik 1998, 2007a). The relatively rich conodont faunas include also Aulacognathus sp. n. (Fig. 5).

The Avaste section

The section is located about 8 km west of the Kivi-Vigala settlement in western Estonia (Figs 1, 6). The strata sampled for conodonts are exposed in shallow gullies just opposite Jarsu farmhouse. The gullies are cut in the upper part of a steep, up to 10 m high terrace which is an ancient coastal cliff of the Litorina Sea, now completely buried and covered by vegetation (Kessel & Raukas 1967). No continuous section is available, but small intervals are exposed in the upper half of the slope. An attempt to clean a section at the base of the slope was unsuccessful, and only two samples from the upper half and the top of the slope were studied (Fig. 6).

The strata sampled are represented by grey, more or less argillaceous dolomitized marlstones. No macrofauna has been found. The beds exposed in the Avaste section have previously been considered to correspond to the Paramaja Member of the Jaani Stage and, accordingly, to be of early Wenlock (Sheinwoodian) age (Aaloe 1961, 1970). The samples processed from this section yielded a conodont fauna, most significantly including P. a. lithuanicus Brazauskas and Aspelundia? ex gr. fluegeli (Walliser), and lacking Ozarkodina polinclinata (Pollock, Rexroad & Nicoll) (Fig. 6).

[FIGURE 4 OMITTED]

Sections on the western end of the Saastna Peninsula

The Saastna Peninsula is located in western Estonia, between Matsalu Bay in the north and Topu Bay in the south (Figs 1, 7). Several small outcrops, mainly exposed surfaces of bedrock, occur on the coastline around the western end of the peninsula. In some of them, a few decimetres thick sections can be compiled. Several spot-samples have been processed from these outcrops (in Fig. 7 the samples are arranged in their probable stratigraphic order).

Along the northwestern coast of the Saastna Peninsula the uppermost Velise Formation, represented by calcareous marlstones and argillaceous limestones, is exposed. The strata are rich in fine bioclastic material, light-coloured ooids, and pyrite. In some beds below sea level, large (up to 2-3 cm) euhedral crystals of pyrite occur. The strata are bioturbated and partly dolomitized. In these outcrops the coral Palaeocyclus porpita Lamark has been found. The rich conodont faunas of these strata are characterized by the occurrences of P. a. amorphognathoides, Apsidognathus walmsleyi Aldridge, Aps. ruginosus, O. polinclinata polinclinata (Pollock, Rexroad & Nicoll), and N. sensitiva (Fig. 7; samples M-853, M-852, M-1811).

Two main types of rock occur in the exposures along the southern coast of the peninsula (samples M-1809 and M-1810; Fig. 7). The lower part of the succession (sample M-1810) is composed of intercalations of grey argillaceous thin-bedded limestone and argillaceous to calcareous marlstone. The rock is bioturbated and contains fine bioclastic material, pyrite aggregates of various sizes, and rare fragments of halysitid corals and of cephalopods. Ooids have not been found in these strata. The calcareous interval is followed by monotonous grey argillaceous marlstone (sample M-1809). The conodont fauna in these strata differs completely from that in outcrops along the northern coast of the peninsula (Fig. 7) and is dominated by Panderodus equicostatus (Rhodes). Walliserodus sp. n. b, characteristic of Telychian strata (Mannik 2007a), is replaced here by Walliserodus sp. n. c. Ozarkodina excavata (Branson & Mehl) is common. Most of the taxa identified in older strata are missing.

[FIGURE 5 OMITTED]

[FIGURE 6 OMITTED]

[FIGURE 7 OMITTED]

DISCUSSION

All studied sections yielded rich conodont faunas of specific composition, allowing precise dating of the exposed strata. The three outcrops just east of the Valgu settlement are characterized by the occurrence of P. eopennatus ssp. n. 1 (Figs 2, 3, 8A-C) and, accordingly, correspond to the P. eopennatus ssp. n. 1 Zone sensu Mannik (2007a) (Fig. 9). In the Valgu-1 section (Valgu drainage canal) the lower boundary of the zone is exposed in the uppermost Rumba Formation. The boundary is marked by a pyritized discontinuity surface suggesting a gap below this level, which may also account for the abrupt appearance of the rich P. eopennatus ssp. n. 1 Zone conodont fauna in the section. The single sample just below the discontinuity surface contains only two poorly preserved conodont specimens, one of which was identified as Panderodus cf. unicostatus and the other as Distomodus cf. staurognathoides. These strata probably correspond to the D. staurognathoides Zone (Figs 2, 9).

At the boundary between the D. staurognathoides and P. eopennatus ssp. n. 1 zones the abundance of conodont specimens increases abruptly, reaching many hundreds to more than a thousand per 1 kg of rock. Also, many taxa appear, including P. eopennatus ssp. n. 1 (Fig. 8A-C), Astropentagnathus irregularis (Fig. 8E), Oulodus? sp. n. A Over & Chatterton (Fig. 8D, F-I), Aulacognathus kuehni (Fig. 8J), Ozarkodina polinclinata estonica Mannik (Fig. 8K), Apsidognathus tuberculatus Walliser (represented in this interval by Aps. tuberculatus ssp. n. 1; Fig. 8M, N, P), and Aps. milleri (Over & Chatterton) (Fig. 8L, R). Astropentagnathus irregularis disappears, as in Valgu-1 and Valgu-2, just below the lowermost, thick double(?) bentonite (Figs 2, 3). The level of disappearance (extinction) of Astr. irregularis marks Datum 1 of the Valgu Event sensu Mannik (2007b). The strata above this level correspond to the uppermost P. eopennatus ssp. n. 1 Zone, as indicated by the occurrence here of morph 5 of the Pa element of P. eopennatus ssp. n. 1 of Mannik (1998) (Fig. 8A-C). The upper boundary of the P. eopennatus ssp. n. 1 Zone is not exposed in the Valgu sections.

The abrupt appearance of many new conodont taxa and rapid increase in the number of conodont specimens at the lower boundary of the P. eopennatus ssp. n. 1 Zone evidently indicates a next (after that marking the lower boundary of the sequence) major flooding event in Sequence 4 (S4) sensu Harris et al. (2005). However, the most distinct lithological change occurs a little higher in the section, at the boundary between the Rumba and Velise formations (between samples M-1962 and M-882 in the Valgu-1 section; Fig.2). The succession of events in this interval (i.e. abrupt appearance of rich P. eopennatus ssp. n. 1 Zone fauna, followed by lithological change at the formational boundary) can be observed in all studied sections in Estonia (e.g. Mannik 2003, 2007a; Rubel et al. 2007). It seems possible that, in terms of sequence stratigraphy, the strata of the Rumba Formation formed during the initial stage of the transgression above the S3/S4 boundary, i.e. they correspond to the Lowstand Systems Tract of sequence S4. If so, then one of the levels discussed above (the boundary between the Rumba and Velise formations?) most probably correlates with the Transgressive Surface in the sequence.

Faunas from the Velise-Korgekalda section are characterized by P. a. angulatus (Fig. 8O, Q, S, U, V, W; Fig. 4), the total range of which corresponds to the P. a. angulatus Zone (Mannik 2007a). Apsidognathus tuberculatus ssp. n. 3 (Fig. 8T, X-Z, BB-DD) indicates that these strata correspond to the lower subzone of the zone (Fig. 9). Judging from the morphologies of the elements of P. a. angulatus [typical [Sc.sub.2] and [Pb.sub.2] elements of the taxon (Fig. 8Q, V) are accompanied by morphologies characteristic of P. eopennatus (Fig. 8S, W)] and Aps. tuberculatus ssp. n. 3 [typical lyriform elements of this taxon (Fig. 8DD) occur together with specimens bearing features characteristic of the older subspecies Aps. tuberculatus ssp. n. 2 (Fig. 8BB, CC)], it is most probable that the lower boundary of the P. a. angulatus Zone lies not far (just?) below the lowermost sample in the section.

[FIGURE 8 OMITTED]

[FIGURE 9 OMITTED]

[FIGURE 10 OMITTED]

The age of the strata exposed in the Jadivere section has been problematic for a long time. Aaloe (1961) assigned these strata, as well as those in the Avaste section (see below), to the Paramaja Member of the Jaani Stage (Sheinwoodian in age). Later, based on the identification of P. amorphognathoides in the Jadivere section, Klaamann (1984a) dated the marlstones here as of latest Llandovery-earliest Wenlock age. Restudy of the section and collections of conodonts revealed that these strata correspond to the P. a. lennarti Zone (to an interval in the upper part of the Adavere Stage, Telychian; Figs 5, 9). The most characteristic conodonts in this section are P. a. lennarti Mannik (Fig. 8AA) and Aulacognathus sp. N. (Fig. 8EE, FF). So far, the latter taxon has not been found below the P. a. lennarti Zone in Estonia, and there are no data about its occurrence in other parts of the world. Aulacognathus sp. n. disappears close to the upper boundary of the zone, probably in the basal part of the overlying P. a. lithuanicus Zone.

As indicated above, previously the strata in the Avaste section have also been assigned speculatively, based only on their lithological composition, to the Jaani Stage (Sheinwoodian). However, conodont data indicate that these strata are considerably older and correspond to the P. a. lithuanicus Zone (upper part of the Adavere Stage, i.e. to the upper Telychian; Figs 6, 9). The faunas in two samples from the middle and uppermost parts of the section are typical of the zone, being characterized by the occurrence of the nominal taxon, P. a. lithuanicus (Fig. l0A-C) and a total lack of O. polinclinata (which is also very characteristic of the zone). The occurrence here of Aps. ruginosus (Fig. IOD, F) probably indicates that the uppermost part of the P. a. lithuanicus Zone is exposed in the section. Apsidognathus ruginosus, as known to date, appears just below the boundary between the P. a. lithuanicus and P. a. amorphognathoides zones.

Two sets of samples were studied from the outcrops at the western end of the Saastna Peninsula (Fig. 7). The three samples from the northern coast (M-852, M-853, and M-1811; Fig. 7) all yielded rich P. a. amorphognathoides Zone faunas, characterized by the occurrence of P. a. amorphognathoides (Fig. 10V, W), O. polinclinata polinclinata (Fig. 10J), Aps. ruginosus Fig. 10E, G-I, M), Aps. walmsleyi (Fig. lOP), and Walliserodus sp. n. b (Fig. IOK, L, N, Q-S). Among the specimens of Pa elements of P. a. amorphognathoides there are morphologies characteristic of Population 4 sensu Mannik (1998) of the taxon (Fig. 10V), indicating that these strata correlate with the Upper subzone of the P. a. amorphognathoides Zone. This agrees with the occurrence of Nudibelodina sensitiva in these samples, which dates this level older than the Ireviken Event (Fig. 9).

The two samples (M-1809 and M-1810) from the southern coast of the Saastna Peninsula yielded low-diversity faunas of the Upper Kockelella ranuliformis Zone (Figs 7, 9). Most characteristic of these faunas is the occurrence of K. ranuliformis (Walliser) (Fig. 10AA), Ozarkodina excavata (Branson & Mehl), Panderodus equicostatus (Rhodes) (Fig. 10X-Z, BB, CC), and Walliserodus sp. n. c (Fig. 10O, T, U).

As revealed by the data above, at present no information is available from an interval corresponding to five conodont zones, from the Lower Pseudooneotodus bicomis Zone below up to the Lower K. ranuliformis Zone (Fig. 9). Considering that the average southward dip of strata is about 2.5-3.5 m per 1 km in Estonia, it can be assumed that the unexposed interval between outcrops on the northern and southern coasts of the Saastna Peninsula is about 1 m thick. Such a small thickness of the strata corresponding to the Ireviken Event on the Saastna Peninsula agrees with data from core sections from western mainland Estonia and the islands in the Muhu Strait (e.g. Hints et al. 2006; Rubel et al. 2007), indicating that the Llandovery-Wenlock boundary interval is highly condensed in this region. Some gaps cannot be excluded.

The boundary between sequences S4 and SS lies in this unexposed interval. The strata exposed along the northern coast of the peninsula, being represented by dolomitized calcareous marlstones-argillaceous limestones with ooids, evidently correspond to the topmost S4 (top of the Highstand Systems Tract) in the region. On the southern coast of the peninsula, the lowermost part of SS is exposed. It is not yet possible to tell the precise level of the sequence boundary in terms of conodont biostratigraphy--below or within the Ireviken Event.

ACKNOWLEDGEMENTS

I would like to thank the referees Prof. R. J. Aldridge (University of Leicester, U.K.) and Dr H. Nestor (Institute of Geology at TUT, Estonia) for very valuable comments, and Dr V. Mikli for SEM assistance. The study was supported by the Estonian Science Foundation grant No. 7138.

Received 6 March 2008, accepted 6 May 2008

REFERENCES

Aaloe, A. 1961. Stratigraphy of the Jaani Stage ([J.sub.1]). Geoloogia Instituudi Uurimused, VI, 13-28 [in Russian, with English summary].

Aaloe, A. 1970. The Jaani Stage. In Silur Estonu [The Silurian of Estonia] (Kaljo, D., ed.), pp. 243-252. Valgus, Tallinn [in Russian, with English summary].

Bischoff, G. C. O. 1986. Early and middle Silurian conodonts from midwestern New South Wales. Courier Forschungsinstitut Senckenberg, 89, 1-337.

Einasto, R., Nestor, H., Kala, E. & Kajak, K. 1972. Correlation of the upper Llandoverian sections in west Estonia. Eesti NSY Teaduste Akadeemia Toimetised, Geoloogia, 21, 333-343 [in Russian, with English summary].

Harris, M., Sheehan, P., Ainsaar, L., Hints, L., Mannik, P., Nolvak, J. & Rubel, M. 2005. The Lower Silurian of Estonia: facies, sequences and basin filling. In The Sixth Baltic Stratigraphical Conference, August 23-25, St. Petersburg, Russia (Koren, T., Evdokimova, I. & Tolmacheva, T., eds), pp. 30-33. VSEGEI, St. Petersburg.

Hints, O., Killing, M., Mannik, P. & Nestor, V. 2006. Frequency patterns of chitinozoans, scolecodonts and conodonts in the upper Llandovery and lower Wenlock of the Paatsalu core, western Estonia. Proceedings of the Estonian Academy of Sciences, Geology, 55, 128-155.

Jeppsson, L. 1997. A new latest Telychian, Sheinwoodian and Early Homerian (Early Silurian) Standard Conodont Zonation. Transactions of the Royal Society of Edinburgh: Earth Sciences, 88, 91-114.

Jurgenson, E. 1964. Silurian metabentonites of the Estonian S.S.R. In Litologiya paleozojskikh otlozhenu Estonu [Lithology of Palaeozoic Deposits in Estonia] (Baukov, S., ed.), pp. 87-100. Academy of Sciences of the Estonian SSR, Institute of Geology, Tallinn [in Russian, with English summary].

Jurgenson, E. 1966. Litologiya llandoverijskikh otlozhenu Estonu [Lithology of Llandoverian Beds in Estonia]. Academy of Sciences of the Estonian SSR, Institute of Geology, Tallinn, 65 pp. [in Russian, with English summary].

Kaljo, D. 1970. The Adavere Stage. In Silur Estonu [The Silurian of Estonia] (Kaljo, D., ed.), pp. 232 243. Valgus, Tallinn [in Russian, with English summary].

Kessel, H. & Raukas, A. 1967. Pribrezhnye otlozheniya Antsilovogo ozera i Litorinovogo morya v Estonu [The Deposits of the Ancylus Lake and Littorina Sea in Estonia]. Valgus, Tallinn, 134 pp. [in Russian, with English summary].

Klaamann, E. 1984a. Locality 5 : 4 Jadivere outcrop. In International Geological Congress, XXPII Session, Estonian Soviet Socialist Republic, Excursions: 027, 028 Guide book (Kaljo, D., Mustjogi, E. & Zecker, L, eds), p. 62. Academy of Sciences of the Estonian SSR, Tallinn.

Klaamann, E. 1984b. Locality 5 : 5 Outcrops in the Valgu village. In International Geological Congress, XXVII Session, Estonian Soviet Socialist Republic, Excursions: 027, 028 Guidebook (Kaljo, D., Mustjogi, E. & Zecker, L, eds), pp. 624. Academy of Sciences of the Estonian SSR, Tallinn.

Mannik, P. 1998. Evolution and taxonomy of the Silurian conodont Pterospathodus. Palaeontology, 41, 1001-1050.

Mannik, P. 2003. Distribution of conodonts. In Ruhnu (500) Drill Core (Poldvere, A., ed.), Estonian Geological Sections, 5, 17 23.

Mannik, P. 2007a. An updated Telychian (Late Llandovery, Silurian) conodont zonation based on Baltic faunas. Lethaia, 40, 450.

Mannik, P. 2007b. Some comments on the Telychian-early Sheinwoodian conodont faunas, events and stratigraphy. Acta Palaeontologica Sinica, 46 (Suppl.), 305-310.

Nestor, H. 1990. Locality 9:1. Silurian sequences at Sarghaua field station. In Field Meeting Estonia 1990, An Excursion Guidebook (Kaljo, D. & Nestor, H., eds), pp. 184-186. Estonian Academy of Sciences, Tallinn.

Nestor, H. 1997. Silurian. In Geology and Mineral Resources of Estonia (Raukas, A. & Teedumae, A., eds.), pp. 89-105. Estonian Academy Publishers, Tallinn.

Nestor, H. & Einasto, R. 1997. Ordovician and Silurian carbonate sedimentation basin. In Geology and Mineral Resources of Estonia (Raukas, A. & Teedumae, A., eds), pp. 192-204. Estonian Academy Publishers, Tallinn.

Rosenstein, E. 1939. Adavere lademest (Silur) Laane-Eestis [About the Adavere Stage (Silurian) in Western Estonia]. Eesti Loodus, 4/5, 136-140 [in Estonian, with English summary].

Rubel, M., Hints, O., Mannik, P., Meidla, T., Nestor, V., Sarv, L. & Sibul, I. 2007. Lower Silurian biostratigraphy of the Vurelaid core, western Estonia. Estonian Journal of Earth Sciences, 56, 193-204.

Peep Mannik

Institute of Geology at Tallinn University of Technology, Ehitajate tee 5, 19086 Tallinn, Estonia; [e-mail]