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Facies

, 66:1 | Cite as

Algae, calcitarchs and the Late Ordovician Baltic limestone facies of the Baltic Basin

  • Björn KrögerEmail author
  • Amelia Penny
  • Yuefeng Shen
  • Axel Munnecke
Open Access
Original Article
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Abstract

The Late Ordovician succession of the Baltic Basin contains a characteristic fine-grained limestone, which is rich in calcareous green algae. This limestone occurs in surface outcrops and drill-cores in an extensive belt reaching from Sweden across the Baltic Sea to the Baltic countries. This limestone, which is known in the literature under several different lithological names, is described and interpreted, and the term “Baltic limestone facies” is suggested. The microfacies, from selected outcrops from the Åland Islands, Finland and Estonia, consists of calcareous green algae as the main skeletal component in a bioclastic mudstone-packstone lithology with a pure micritic matrix. Three types of calcitarch, which range in diameter from c. 100–180 μm, are common. Basinward, the youngest sections of the facies belt contain coral-stromatoporoid patch reefs and Palaeoporella-algal mounds. The Baltic limestone facies can be interpreted as representing the shallow part of an open-marine low-latitude carbonate platform.

Keywords

Lithographic limestone Shallow-water carbonates Dasycladacales Calcitarch Ordovician 

Introduction

The Ordovician succession of the Baltic region is characterized by a drastic change from siliciclastic sediments and cold-water carbonates in the Early Ordovician to warm-water carbonates, with reefs and mud mounds, with little siliciclastic input, in the Late Ordovician. A unique and enigmatic lithofacies within the Late Ordovician warm-water carbonates consists of a dense, hard, stylolitic, fine-grained limestone, with a specific conchoidal fracture and very even texture. Commonly the limestone has been referred to as “calcilutitic”, “aphanitic” or “lithographic” (e.g. Jaanusson and Martna 1948; Spjeldnæs and Nitecki 1994; Hints et al. 2005). It is best described as a fine-grained bioclastic carbonate mudstone—packstone. Its most conspicuous and commonly most abundant skeletal elements are fragments of benthic green algae (e.g. Wiman 1893; Stolley 1896, 1897; Martna 1955; Hucke and Voigt 1967; Kozlowski and Kazmierczak 1968; Vingisaar 1971; Põlma 1972, 1982; Kõrts et al. 1990; Spjeldnæs and Nitecki 1994; Hints et al. 2005).

In view of its relatively wide spatial distribution (Fig. 1) and stratigraphic range (Fig. 2), and its widespread occurrence as erratic boulders across northern Europe, this lithofacies is known under various lithostratigraphical names, including Baltic or Östersjö limestone (Wiman 1893; Thorslund 1960), Knyckelkalk or Masur limestone (Warburg 1910), Ostseekalk or Paläoporellakalk (Hucke and Voigt 1967), Rägavere Formation (Hints and Meidla 1997), Saunja Formation (Männil 1958), and Slandrom limestone (Jaanusson and Martna 1948), and various units of the eastern Baltic Pirgu Stage, such as the Moe Formation (Hints et al. 2005). These names do not necessarily reflect well-defined lithostratigraphical units, but in some cases just denominate the characteristic lithology (as in Baltic limestone or Palaeoporella limestone).
Fig. 1

Map of Baltoscandia showing the maximum extent of the Baltic limestone facies and localities in southwestern Finland and Estonia discussed herein (based on Männil 1966; Winterhalter 1972; Jaanusson 1976; Raukas and Teedumäe 1997; Hints et al. 2005; Calner et al. 2010). Note: occurrences of the Slandrom Limestone in Sweden are not depicted for simplicity

Fig. 2

Schematic overview on the geographic and stratigraphic extent of selected lithostratigraphic units of the Baltic limestone facies (based on Jaanusson and Martna 1948; Merrill 1980; Tynni 1982; Ainsaar 1991; Hints and Meidla 1997; Hints et al. 2005; Ebbestad and Högström 2007; Calner et al. 2010). The hatched line marks non-established borders. Stars represent reef occurrences, filled stars with green algae present

Herein, the term “Baltic limestone facies” is used to cover all these names. Baltic limestone lithologies occur stratigraphically in an interval that ranges from the Keila Regional Stage (late Sandbian Stage) towards the higher Pirgu Stage (late Katian Stage or lowermost Hirnantian) (Fig. 2). They are stratigraphically most persistent in a wide belt, which reaches from Bothnian Bay and the Åland Islands in the west to northern Gotland in the south and the Saaremaa Island and central Estonia in the east (Fig. 1). The greatest extension of this facies towards the south was reached during the time of Nabala and Rakvere regional stages. During this time the Slandrom Formation extended as far west as to the Siljan area in central Sweden (e.g. Calner et al. 2010) and the Saunja Formation as far south as central Lithuania (Männil 1966).

One particular feature of the Baltic limestone facies is its proximity to mud mounds and reefs, which are especially widespread and thick during the Pirgu Stage (Kröger et al. 2016b) but are also reported from the Rakvere Stage, as in the Puhmu drill core from central Estonia (Kaljo et al. 2017). Notably, green algae such as Palaeoporella, Vermiporella and dasycladaceans are abundant in these structures and in some places they are the dominant skeletal element (Jux 1966; Kröger et al. 2016a, b).

Here, a microfacies analysis of limestone samples from selected localities from the Baltic limestone facies belt is presented. The aim of this study is to understand better the formation processes that led to the widespread deposition of pure limestones in the region. The potential role of algae in producing the Baltic limestone facies is investigated. Spherical calcareous microfossils, which have been mentioned but not previously figured (Spjeldnæs and Nitecki 1994: p. 270), are abundant in some samples. These fossils are determined as calcitarchs and interpreted as algal spores. Calcitarchs are spherical calcareous microfossils (< 550 μm) of unknown and varied biological affinities, previously often subsumed under the more diffuse and less well defined term “calcisphere” (Versteegh et al. 2009). They have been implicated in regional-scale micrite production in later Palaeozoic marine basins, and here we assess the possibility that they were important carbonate sources in the Ordovician Baltic Basin.

Material and sampling

All samples are from Late Ordovician limestones of the peri-cratonic Baltic Basin, of northeastern Europe. The basin is situated between the Scandinavian shield in the present north and the Sarmatian shield in the present south (Sliaupa et al. 2006) and records a thick early Palaeozoic succession. The Ordovician sediments of the basin have been spatially subdivided by faunal and lithological differences into a number of zones, termed “confacies belts” (Männil 1966; Jaanusson 1976). The confacies belts roughly correspond to the spatial lithofacies distribution along a proximal—distal gradient (e.g. Männil 1966; Jaanusson 1982; Raukas and Teedumäe 1997; Harris et al. 2004; Kröger et al. 2016b). Samples examined here are from drill cores, surface outcrops and erratic boulders of the Åland Islands, Finland and from western and southern Estonia (Fig. 1).

A number of samples were analysed as polished surfaces, in thin-sections under optical light, and under scanning electron microscopy (SEM). For SEM analysis the samples where polished and slightly etched following the methods described in Munnecke et al. (2000).

Tranvik-Lumparn borehole nr. 6, Åland Islands, Finland

The drilling of this core took place during a mainly off-shore drilling campaign of the Partek company (now Nordkalk Oy Ab) in 1964, which produced c. 25 drill-cores from the Lumparn bay area. Core no. 6 was drilled in northern Lumparn Bay, ~ 250 m south of the tip of Tranviknäs (60°10′20.24″N, 20°9′55.55″E) and has been previously mentioned or briefly described (Merrill 1980; Tynni 1982). The core covers a thickness of 34.5 m, but the stratigraphy of the section cannot be resolved in detail because of a lack data.

The topmost beds of borehole no. 6 are composed of a nodular, reddish fine-grained limestone with a Baltic limestone lithology, rich in Vermiporella with ~ 1 mm diameter branched thalli. The succession contains several strongly brecciated horizons, which are almost mylonitic with cm-sized angular intraclasts. The reddish nodular Baltic limestone lithology ranges down to the base of the preserved part of the core at 33 m, where it is rich in recrystallized microgastropods and Vermiporella sp. Generally, the section represents a metre-scale to tens of metre-scale alternation between reddish, argillaceous and lime-rich sections with calcareous algal, gastropod mudstone—wackestone lithologies. Merrill (1980), who described conodonts from older sediments in the Lumparn drill-cores, found none in the drill-core no. 6 samples. Tynni (1982) described the long ranging (upper Haljala Regional Stage, Sandbian–Juuru Regional Stage, Rhuddenian) Tasmanites aff. verrucosus from 21.2 m as the only determinable acritarch and Leiosphaeridia from the argillaceous interval 21.8–19.9 m. In Estonia Leiosphaeridia is not known from Ordovician beds younger than the Keila Regional Stage (uppermost Sandbian) (which is traditionally used as a stratigraphically significant pattern, e.g. Hints et al. 2016), which gives an upper Sandbian (Jõhvi-Keila Stage) age constraint for the 21.2–19.9 m interval. An upper age constraint for borehole no. 6 can be given from the nearby Tranvik-Lumparn borehole no. 7 and the Tranvik Udde outcrop, which produced Amorphognathus superbus zone, Rakvere-Nabala Regional Stage conodonts (Merrill 1980).

Erratic boulders from southwestern Finland

Pleistocene erratic boulders with Baltic limestone lithologies are among the most widespread and abundant type of Palaeozoic erratics in southwestern Finland. The age and dispersal of these boulders have been described in detail (Uutela 1989; Nõlvak et al. 1995). Two types of Baltic limestone have been distinguished, an older yellowish-grey and a younger reddish-grey variant. A Rakvere Stage age was determined for both types of boulder based on acritarchs, chitinozoans and ostracods. Four samples have been collected from Åland Island: the Jomala area, samples A3, A5, from 60°9′32.90″N, 19°59′6.39″E; from Önningby, sample A7 (= FMNH-P6698), from 60°07′01″N, 20°00′29.8″E; from Svibyviken, Mariehamn, sample A1, from 60°6′03″N, 19°55′23″E (Fig. 3a). Two samples came from Kustavi, Vakka-Suomen county, southwestern Finland, sample A6 (= FMNH-P23586), and A8 (= FMNH-P28717) from 60°32′42″N, 21°21′19″E. Boulders with macrofossils were selected. Sample A6 contains Hedstroemina inaequiclina (Alichova), which is known from Oandu and Rakvere Stage levels from Estonia (Hints et al. 2016). Samples A2, A5, and A8 contain Hedstroemina sp. The age of erratic boulder samples can only be approximated as between late Keila to Nabala stages based on drill-core data (see above), brachiopod fossils and the few published analyses of similar boulders.
Fig. 3

Polished samples of examples of Baltic limestone facies. a Mudstone lithology, Baltic Limestone, Lumparn drillcore no. 6, Åland Islands, Finland, depth 11.70 m (sample Lump-6.11), early Katian. b Wacke-packstone lithology, sample Vm02, Võhma drill-core, Estonia, depth 220.55 m, Rakvere Stage, early Katian. Note the syndepositional cracks (see text for discussion). c Packstone lithology, sample Vm06, Võhma drill-core, Estonia, depth 218.78 m, Rakvere Stage, early Katian. Note the heavy bioturbation. Similar scale in all figures

Hoitberg reef, Vormsi Island, Estonia

The Hoitberg reef is a natural surface outcrop in the centre of western Vormsi Island, Estonia, at 59°0′16″N, 23°10′58″E. The outcrop consists of an overgrown 5–10 m high elongate hill with a width of c. 30 m, length of c. 80–100 m, and a maximum expansion in NNW/SSE -direction. The reef is lithologically embedded within an algal-rich fine-grained limestone of the Moe Formation (Hints et al. 2005). Several large (metre-scale) blocks of the reef are exposed mostly on its northern part and provide insight into the composition of the reef core and flanks. The core consists of a coral-boundstone with a non-skeletal matrix content of 56–72%. The most abundant skeletal reef-builder is the heliotid tabulate Eocatenipora, which comprises 18–41% of the rock volume in the sampled areas. Stromatoporoids and bryozoans, mostly dendroid growth forms, were minor skeletal reef-builders with less than 5% of the rock volume. The matrix consists of mudstone—wackestone lithologies, in several places with a fenestral-microbial texture. The skeletal components of the matrix are Vermiporella algae and ostracods, calcitarchs, sponge spicules and bryozoan fragments are abundant.

Kaugatuma 509 borehole, Saarema Island, Estonia

The Kaugatuma 509 drill hole is situated close to the north-east coast of the Sõrve Peninsula at 58°7′25.572″N, 22°11′39.4794″E, on the southern Saaremaa Island, Estonia. The core is ~ 466 m deep and ranges from the Upper Silurian down to the Middle Ordovician. Parts of the Ordovician section have been previously described and figured (Põlma 1973; Oraspõld 1982; Oraspõld and Kala 1982; Nõlvak 1989; Kaljo 2001; Brenchley et al. 2003; Ainsaar et al. 2010). Herein, two samples are described: Kaug-2 from 411.38 m, Rägavere Formation, Rakvere Stage, and Kaug-3, 387.6 m from the upper part of the Saunja Formation, Nabala Stage. The top of the Keila Stage Kahula Formation at Kaugatuma 509 is a distinct hardground at 413.7 m, which marks an abrupt facies change from greenish-grey argillaceous wackestone toward a decimetre-scale intercalation of nodular fine-grained limestone and dark grey argillaceous interlayers of the Tõrremägi Member. The Tõrremägi Member grades toward the top into pure pale pinkish-grey nodular stylolitic, fine-grained limestone with a bioclastic mudstone-wackestone lithology. From 413.1 to 411.1 m a pure fine-grained limestone with bioclastic mudstone-wackestone lithology of the Piilse Member prevails. Its top, at 411.1 m, is a pyrite stained planar hardground with distinct Trypanites burrows. Sample Kaug-2 is from 0.18 m below this hardground. The overlying Paekna Formation of the Nabala Stage is again an alternation of decimetre-scale intercalation of nodular fine-grained limestone and dark green argillaceous interlayers. The top of the Paekna Formation is relatively abrupt, with a hardground forming the base of the Saunja Formation at 407.4 m. The Saunja Formation consists of a massive, pure, pale pinkish-grey bioturbated stylolitic, fine-grained limestone with bioclastic mudstone-wackestone lithology; its top is a karstic, heavily burrowed and eroded surface at 387.1 m. Sample Kaug-3 is from 0.5 m below the top Saunja hardground.

Niibi trench, western Estonia

The outcrop is a shallow trench on both sides of the unpaved road that leads from Niibi hamlet to road 16,122, c. 150–400 m west of Niibi, Lääne county, western Estonia at 59°2′29.60″N, 23°39′28.89″E. The trench exposes the top of a number of small patch reefs, each with a maximum diameter of less than 5 m. Similar reefs also crop out on a fallow land ~ 50 m south of the road and have been described from a now nearly overgrown quarry ~ 180 m to the west of the road. Fossils collected from these and probably from other shallow reef outcrops in the direct vicinity have been described (Kaljo 1961; Nestor 1964; Klaamann 1966; Preobrazhensky and Klaamann 1975).

The reefs occur within the Moe Formation, Pirgu Stage, late Katian. Some of these patch reefs are covered and surrounded by a coarse, partly argillaceous greenish echinoderm packstone—echinoderm grainstone. The reefs themselves are composed of a matrix-rich coral-boundstone. The matrix has a skeletal mudstone—wackestone lithology, in several places with a fenestral-microbial texture. The dominant skeletal element of the boundstone is the heliotid coral Eocatenipora (see Klaamann 1966) and locally large colonies of Sarcinula. Stromatoporoid colonies are common (see Nestor 1964). The most abundant skeletal elements in the matrix are dasycladal green algae, echinoderm ossicles and fragments of bryozoan skeletons.

Valga 10 borehole, southern Estonia

The Valga 10 drill-hole is located in southern Estonia, near the Latvian border at 57°48′14.4″N, 26°04′39″E on the NE outskirts of the town of Valga. The section was described in detail in a monographic treatment (Põldvere 2001); it is 424.4 m deep and penetrates Quaternary, Devonian, Silurian and Ordovician sediments. Since 2001 individual sections of the core have been described and discussed in numerous publications from which a few are relevant herein because they give additional age constraints and lithological information (Ainsaar and Meidla 2001; Nõlvak and Bauert 2006; Ainsaar et al. 2010). Sample Vg-1 is from 379.65 m, from 0.25 above the base of the Rägavere Formation, Rakvere Stage. The Rägavere Formation, ~ 6.7 m thick at Valga 10, is unconformity bounded and consists of greenish to brownish, wavy thin-bedded fine-grained limestone with a skeletal mudstone lithology, and with finely dispersed pyrite and dolomite mainly in its upper parts. The limestone is cracked and contains predominantly sub-centimetre to centimetre-thick sparite-filled veins which contain geopetal argillaceous crystal dolomitic silt (see also Ainsaar and Meidla 2001) which we interpret as palaeokarst following Calner et al. (2010).

Võhma borehole, central Estonia

The Võhma drill-hole is located south of the parish Võhma, Viljandi county, central Estonia, at 58°36′44.136″N, 25°33′34.056″E. The drill-core section is 438 m deep with a stratigraphic range from the Proterozoic crystalline basement up to the lower Silurian Adavere Stage. Parts of the section have been described in publications; most relevant are Oraspõld (1982) and Kröger et al. (2016a, b), which cover the parts of the Pirgu Stage. The Pirgu Stage is exceptional at the Võhma drill-core, because it exposes ~ 52 m of a Palaeoporella mud mound.

Here, seven samples, Vm01–Vm07, are analysed ranging stratigraphically from the Rakvere Stage to the upper part of the mound. The samples Vm02 and Vm06 are from 220.55 m and 218.78 m, Rakvere Stage, which ranges in the Võhma drill-core from 221.75 to 214.50 m (Fig. 3b, c). The position of the lower boundary of the Rakvere Stage is not fully resolved because the lithology grades from a predominantly argillaceous decimetre-scale intercalation of greenish-grey nodular fine-grained limestone and dark-grey argillaceous interlayers toward massive pinkish fine-grained limestone in a ~ 0.5 m interval. Here, the notebook no. 6 of Põlma (http://geokogud.info/doi/10.15152/GEO.126) is followed where the boundary is positioned at the base of the lowermost pinkish nodular fine-grained limestone bed. The upper boundary of the Rägavere Formation is a distinct, pyrite-stained hardground, which marks a sharp lithological boundary towards the more argillaceous greenish limestone of the Paekna Formation, Nabala Stage. The limestone of the Rägavere Formation is cracked at some levels and contains predominantly sub-centimetre to centimetre-thick sparite-filled veins containing partly gravitationally filled argillaceous crystal dolomitic silt which is interpreted as a palaeokarst following Calner et al. (2010). Samples from the algal-mud mound, Pirgu Stage, are from depths 144.20 m (Vm04), 155.37 m (Vm03), 160.15 (Vm07); 187.29 m (Vm01) and comprise the two key lithologies of the mound. Samples Vm01 and Vm03 are from fenestral, stromatactis-rich bioclastic wackestone—packstone lithologies and samples Vm04 and Vm07 represent originally algal-rich parts of the mound.

Results

Description of the calcitarchs

Type-I calcitarchs. Small spar-filled spheres, circular in cross-section, with no or a very thin wall. Diameter ~ 100 μm (median, 106 μm; 1. quantile, 80 μm; 3. quantile, 135 μm) (Figs. 4aa–ab, 5e, f). Occur predominantly in mudstone lithologies of the Baltic limestone facies.
Fig. 4

Calcitarchs and other spheroidal microfossils from the Baltic limestone facies, Katian Stage. aaab Type-I calcitarchs. ac–ba Type-II calcitarchs. bb, bc, ca–eb Type-III calcitarchs. Similar scale in all figures. bd Type-III lower right corner, Apidium sp. upper left corner. ec–fb, fc, fd, Apidium sp. aa from Valga 10 drill-core, Estonia, depth 379.65 m (sample Vg-1), Rakvere Stage. ab from Kaugatuma 509 drill-core, Estonia, depth 387.6 m (sample Kaug-3), Nabala Stage. ac from erratic boulder, Svibyviken, Mariehamn, Åland islands, Finland (sample A1), early Katian. ad, bc, ca, da, dd, eb from Võhma drill-core, Estonia, depth 155.37 m (sample Vm03), algal-mud mound, Pirgu Stage. ae, bb, bd, cb-cd, ea, ec, ed, fa, fb, fd from Hoitberg reef, Vormsi island, Estonia (samples H4a–c), Pirgu Stage. ba, ce, db, de from Võhma drill-core, Estonia, depth 144.20 m (sample Vm04), algal-mud mound, Pirgu Stage. dc from Võhma drill-core, Estonia, depth 220.55 m (sample Vm02), Rakvere Stage. fc from Hoitberg reef, Vormsi island, Estonia (sample H3), Pirgu Stage

Fig. 5

Thin-sections of examples of Baltic limestone facies. a Packstone lithology from Võhma drill-core, Estonia, depth 218.78 m (sample Vm06), Rakvere Stage, early Katian. b Wacke-packstone lithology from Võhma drill-core, Estonia, depth 220.55 m (sample Vm02), Rakvere Stage, early Katian. c Wacke-packstone lithology from Kaugatuma 509 drill-core, Estonia, depth 411.38 m (sample Kaug-2), Nabala Stage. d Wacke-packstone lithology from erratic boulder, Svibyviken, Mariehamn, Åland islands, Finland (sample A1), early Katian. e Mudstone lithology from Lumparn drill-core no. 6, Åland Islands, Finland, depth 11.70 m (sample Lump-6.11), Baltic Limestone, early Katian. f Mudstone lithology from Valga 10 drill-core, Estonia, depth 379.65 m (sample Vg-1), Rakvere Stage. Similar scale in all figures, except f. cs calcitarch, e echinoderm ossicle, g gastropod, mp Monilipora sp., o ostracod, rc rugose coral, tr trilobite, um unknown mollusc, vp Vermiporella sp

Type-II calcitarchs. Small spheres with thin, simple wall. Diameter ~ 130 μm (median, 131 μm; 1. quantile, 103 μm; 3. quantile, 174 μm) (Fig. 4ad, ae, ba). Wall thickness ~ 0.05–0.15 of sphere diameter. Occur in most samples of the Baltic limestone facies and in the mounds and reefs.

Type-III calcitarchs. Spheres with wall with radially arranged structures. Diameter c. 180 μm (median, 182 μm; 1. quantile, 159 μm; 3. quantile, 207 μm) (Figs. 4bb–ec, 6a–d). This group comprises three subgroups. A first group has simple radial walls, c. 0.10–0.15 of sphere diameter. A second group has simple thick radial walls with thickness of > 0.2 of sphere diameter that form irregularly shaped internal cavities commonly with radial margins. A third group has a bilayered, thinner outer and thicker inner layer. Commonly the inner layer has twice the thickness of the outer layer. The three groups are not sharply distinguished and their determination depends on fine differences in preservation and the position of the cross section. Occur in most samples of the Baltic limestone facies and in the mounds and reefs. Type-III calcitarchs are most abundant in the reef and mound facies.
Fig. 6

SEM images of the ultrastructure of the Baltic limestone facies, of calcitarchs, and of the microproblematic Ovummurus duoportius Minoura and Chitoku. All images are parallel to bedding surface. a–e Calcitarchs with shell consisting of radially arranged calcite crystals, some with pores (arrows). a O. duoportius preserved within a calcitarch. d O. duoportius, detail of a. f Detail of the micritic matrix, from Valga 10 drill-core, Estonia, depth 379.65 m (sample Vg-1), Rakvere Stage. Note the common pores within the micrite crystals. a–e from Võhma drill-core, Estonia, depth 155.37 m (sample Vm03), algal-mud mound, Pirgu Stage

Description of the microfacies

Baltic limestone, Sandbian—early Katian. The samples from the Baltic limestone range in lithology from mudstone to packstone. The matrix is a very fine homogenous micrite with a weakly floccose texture (Fig. 7). Individual flakes have a size of < 50 μm and are composed of different grain sizes. Finely dispersed pyrite/limonite and organic matter occur in spots (< 1%).
Fig. 7

Close-up of micritic matrix of limestone from Rakvere Stage, Valga 10 drill-core, Estonia, depth 379.65 m (sample Vg-1)

The only non-matrix component in the mudstone lithology consists of round microspar dots (diameter < 50 μm) with diffuse margins and type-I calcitarchs (Figs. 3a, 5e). The skeletal wacke-packstone lithology contains abundant ostracod shell hush and fragments of Moniliporella sp. thalli (Fig. 5d). The thalli are partly strongly disintegrated and marginally micritized. Shell fragments of brachiopods, trilobites and echinoderms occur. The packstone lithology contains predominantly skeletal fragments of Moniliporella sp. and strongly disintegrated and marginally micritized fragments of Vermiporella sp. Few type-I and type-II calcitarchs occur.

Rägavere Formation, Rakvere Regional Stage, early Katian Stage. The samples from the Rägavere Formation range in lithology from mudstone to skeletal packstone. The matrix is similar to the Baltic limestone samples. The skeletal components of the mudstone (sample Vg-1, Fig. 5f) are rare type-I calcitarchs, disintegrated shell fragments of ostracods and monaxial and triaxial sponge spicules. In the wacke-packstone (sample Vm02, Figs. 3b, 5b), dasyclad algae (Moniliporella sp.) are predominant; disintegrated ostracod shell fragments and microgastropods are abundant and a few echinoderm ossicles occur. Type-I and type-III calcitarchs are rare. The sample Vm06 (Figs. 3c, 5a) has a skeletal packstone lithology with c. 50% fragments of green algal skeletons. Fragments of thalli of Vermiporella sp. are predominant, Moniliporella sp. are second abundant. The partly strongly disintegrated fragments are marginally micritized to different degrees. Ostracod shell hash, microgastropods and echinoderm ossicles occur. Type-I and type-II calcitarchs, and brachiopod shell fragments are rare.

Saunja Formation, Nabala Regional Stage, early Katian Stage. Two samples from the Saunja Formation were analysed (samples Kaug-2, Kaug-3) with mudstone–packstone lithologies. The matrix is similar to the Rägavere Formation samples. The mudstone contains only a few echinoderm ossicles and type-II calcitarchs. The skeletal components of the wacke–packstone lithologies contain predominantly fragments of Moniliporella sp. and strongly disintegrated Vermiporella sp. Shell fragments of brachiopods and bryozoans occur; microgastropods and type-II calcitarchs are rare.

Algal-mud mound, Pirgu Regional Stage, late Katian Stage. The algal mound samples from Võhma comprise boundstone to skeletal packstone lithologies with a complex diagenetic history (Fig. 8a–d). The algal-thalli in the boundstone occur only as ghosts with original features preserved at the micritized thallus margins. They are interpreted from size and shape as Palaeoporella sp. and contain gravitational infills of peloidal packstone of crystal silt to micrite, massive sparite and botryoidal cements. The matrix between the thalli ghosts is a peloidal micritic packstone with individual peloid size < 50 μm that contains abundant complete ostracods, bryozoan and echinoderm fragments. Type-III calcitarchs are abundant and type-II calcitarchs occur in the matrix and partly in the infill. The packstone sample contains mostly echinoderm ossicles, fragmented recrystallized shells of molluscs and marginally micritized fragments of Vermiporella sp. and less abundant other dasycladaceans such as Dasyporella sp., Moniliporella sp. and Mastopora sp. Type-II and type-III calcitarchs are abundant. The occurrence of Ovummurus duoportius Minoura and Chitoku 1979, from a Pirgu-age algal-mud mound (Fig. 6a, e, sample Vm03) is, to our knowledge, the oldest record of the microproblematic family Ovummuridae (Munnecke et al. 2000).
Fig. 8

Thin-sections of examples of reef limestone from reefs and mounds of Pirgu age, late Katian, Estonia. a, b Palaeoporella boundstone from Võhma drill-core, Estonia, depth 160.15 m (sample Vm07) c Palaeoporella boundstone from Võhma drill-core, Estonia, depth 144.20 m (sample Vm04). d skeletal intraclastic packstone from Võhma drill-core, Estonia, depth 155.37 m (sample Vm03). e Eocatenipora boundstone with Apidium sp. (sample H4c). f fenestral intraclastic packstone from Hoitberg reef, Vormsi island, Estonia (sample H3). ap Apidium sp., bryo bryozoa indet., cs calcitarch, dc dasycladal algae indet., e echinoderm ossicle, ms Mastopora sp., rc rugose coral, vp Vermiporella sp

Coral-stromatoporoid reefs, Pirgu regional stage, late Katian. The samples from the Hoitberg reef are boundstone to packstone lithologies with the tabulate Eocatenipora vormsiense Klaamann, as the main skeletal component and abundant fragments of bryozoans and ostracod shells as secondary skeletal components (Fig. 8e–f). The matrix of the boundstone consists of a mudstone-wackestone lithology with a clotted fabric and partly with irregular fenestrae that are filled with sparite and a gravitational micritic infill. Type-II and type-III calcitarchs occur. Notably patches and individual thalli of questionable Apidium sp. occur in this matrix. The intraclastic, fenestral packstone lithology is rich in fragments of dasycladaceans, predominantly Vermiporella sp. Type-II and type-III calcitarchs occur. Similar skeletal components and calcitarchs occur also in the matrix of the boundstone and packstone lithologies of the Niibi reefs.

Interpretation

The micritic matrix of the Baltic limestone facies

One of the distinctive features of the Baltic limestone facies is its fine-grained, homogenous micritic matrix. In macroscopic view, patches commonly occur with different colours between pink and yellow, probably tracing bioturbation patterns. These patches are caused by differences in organic matter and skeletal content, or the distribution of finely dispersed pyrite and locally by the occurrence of dolomite, all probably related to minor differences in original porosity. In thin-section, centimetre-sized burrows are commonly preserved with perfect circular cross-sections in a horizontal or subhorizontal direction, which indicate little or no diagenetic compaction of the limestone and hence early lithification. Early lithification is also indicated by swiss-cheese karst features crossing down from the top Rägavere and top Saunja formation surfaces, respectively, and from the uncompressed fossils themselves. Under high magnification the micritic matrix commonly shows flake-like, angular patches or lumps with sizes of less than 50 μm consisting of μm-sized clusters of micrite crystals.

The relatively high abundance of non-disintegrated, marginally micritized dasycladacean thalli among the skeletal fragments in the limestones is evidence for a shallow-water environment with a depositional depth of less than 25 m within the shallow euphotic zone (Granier 2012). This is an environment in which other calcareous green algae could have flourished with less rigid skeletons, such as Acetabularia. Recent calcareous green algae are known to produce 750 g CaCO3/m2 (Acetabularia, Marszalek 1975) to up to 2400 g CaCO3/m2 (Freile et al. 1995). Under SEM several micritic samples exhibit a microporous texture, which is very similar to the one described in Lasemi and Sandberg (1984) and Munnecke et al. (1997), probably representing relics of aragonite needles within a μm-range, and which can be interpreted as representing a texture of an original aragonite-dominated lime-mud (Fig. 6f).

It is, therefore, coherent to assume a green algal, aragonitic origin and rapid recrystallisation of the micritic matrix of the Baltic limestone facies analogous to the diagenetic process known from recent aragonite-dominated tropical platform sediments (Munnecke et al. 1997). Our interpretation is also in accordance with the long-standing opinion that the appearance of a widespread micrite-rich limestone facies is related to the palaeogeographical drift of the Baltica continent toward lower latitudes and warmer climatic conditions (Dronov and Rozhnov 2007; see also Nestor and Einasto 1997).

Comparison and interpretation of Late Ordovician calcitarchs

Few descriptions of Palaeozoic calcitarch occurrences exist. The specimens described and figured herein are unique and differ from previously described forms in terms of size and partly in wall structure. The spores found in situ in the thalli of Late Ordovician Vermiporella sp. are smaller (~ 35 μm, Kozlowski and Kazmierzak 1968). The spherical microfossils from the Silurian Visby and Högklint formations are also generally smaller (< 100 μm, Munnecke and Servais 2008; Servais et al. 2009). The simple-walled spherical microfossils described from the Devonian Choteč and Třebotov formations are similar in general appearance and structure to our type-II calcitarchs but are also smaller (80–120 μm, Berkyova and Munnecke 2010). Late Palaeozoic radiospheres (Kaźmierczak and Kremer 2005) differ in having external spines.

The calcitarchs described herein, show no signs of organic walls in thin-section or under SEM observation and, therefore, cannot be interpreted as calcified acritarchs. However, all three calcitarch groups distinguished herein are close to the size range known from recent calcified spherical non-motile asexual spores (aplanospores) of chlorophyceans, such as Acetabularia (140–185 μm, Marszalek 1975). Notably, all these Ordovician calcitarchs co-occur with green algae and have their mass occurrences, where green algae are abundant. This co-occurrence is not a taphonomic effect of preferred preservation within specifically fine-grained micritic matrix, because calcitarchs occur also in peloidal and intraclastic packstones of the algal-rich reef facies (see above).

The calcitarchs, described herein, occur together with calcified green algae as the most conspicuous skeletal component of the Baltic limestone facies and its associated reefs. It appears likely that the calcitarchs described herein are aplanospores of various green algae, probably of taxa that are not preserved as articulated fossils, like the fast disintegrating Acetabularia. This interpretation is in accordance with the idea that the characteristic fine-grained and homogenous micritic matrix of the Baltic limestone facies originated from aragonitic algal mud.

Comparison of the Baltic limestone facies with similar Palaeozoic carbonates elsewhere

Probably the most similar facies to the Baltic limestone facies can be found in the algal-rich platform carbonates of the Ordos-Basin (northwest China) within the early Katian Beiguoshan Formation (Zheng et al. 2018). Zheng et al. (2018) described a situation with coral-stromatoporoid patch reefs, a platform margin-reef belt and micritic carbonates in a back-reef shallow-water environment, which is rich in dasycladaceans, other green algae, gastropods and crinoids.

Algal-rich massive limestone deposits, algal mounds and reefs are also described from the Katian Lianglitage Formation of the western Tarim Basin (northwest China) and are interpreted as tropical shallow-water carbonates (Zhang et al. 2014; Shen and Neuweiler 2016). Notably the Ordos Basin and the Tarim Basin carbonates contain Vermiporella sp. as the dominant algal constituent, similar to the Baltic limestone facies. Calcitarchs are not described from these northwest China carbonate platforms.

They are described from the micritic limestone of the marl-limestone alternations of the Upper Visby and Högklint formations (latest Llandovery to early Wenlock, Munnecke et al. 1999; Servais et al. 2009). These occurrences are also from a shallow tropical carbonate environment with small patch reefs but differ in lacking the abundant green algal component and in being generally more argillaceous than the massive and pure Baltic limestone facies. The calcitarch bearing Devonian Choteč and Třebotov formations represent different depositional environments ranging from relatively deep to extremely shallow, and do not contain reefs, mounds or green algae.

In conclusion, the Baltic limestone facies appears to be related to time-equivalent tropical shallow platform carbonates, probably reflecting primarily similar climatic conditions such as high temperatures and extremely low terrigenous sediment input.

Conclusions

Along the eastern and northeastern margin of the Baltic Basin a wide facies-belt developed during the Late Ordovician, characterised by an extremely pure limestone with a fine homogenous micritic matrix. The limestone is rich in dasycladacean algae and contains abundant calcitarchs. This algal-rich micritic limestone which comprises several regional chronostratigraphic zones and lithostratigraphic units is combined under the new term “Baltic limestone facies”. Three types of calcitarchs and a number of genera of green algae (Apidium sp., Dasyporella sp., Mastipora sp., Moniliporella, Vermiporella sp.) can be distinguished within the samples analysed in our study. The dasycladaceans indicate an original deposition of the limestone within the shallow euphotic and euryhaline zone under low-latitude climatic conditions. Basinward the limestone contains coral-stromatoporoid patch reefs and Palaeoporella-algal mounds. The Baltic limestone facies can be interpreted as representing the shallower part of an open-marine carbonate platform.

Notes

Acknowledgements

Open access funding provided by University of Helsinki including Helsinki University Central Hospital. BK is grateful to Susan Scholze and Duncan Matthews (Helsinki) for support with data compilation and preparation of samples. We are grateful to Kenneth Fjäder and Gerhard Hakkarainen (Nordkalk Oy, Parainen) for access to Åland drill cores. Ursula Toom (Tallinn), Mare Isakar (Tartu) and Gennady Baranov (Tallinn) where wonderful field work companions in Estonia, and Dina Schultze and Radoslaw Michallik (Helsinki) provided technical assistance and useful discussions. Many thanks also to Olle Hints (Tallinn) for general support during field work in Estonia. BK and AP were funded by the Academy of Finland. This is a contribution to the IGCP Project 653 ‘The Onset of the Great Ordovician Biodiversification Event’.

References

  1. Ainsaar L (1991) Settetsüklite kasutamine karbonaatsete läbilõigete detailsel korrelatsioonil Pääsküla kihistiku (DIIP) näitel Põhja-Eestis. Tartu Ülikooli toimetised 934:3–11Google Scholar
  2. Ainsaar L, Meidla T (2001) Facies and stratigraphy of the Middle Caradoc mixed siliciclastic-carbonate sediments in Eastern Baltoscandia. Proceedings of the Estonian Academy of Sciences, Geology vol 50: pp 5–23Google Scholar
  3. 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. Palaeogeogr Palaeoclimatol Palaeoecol 294:189–201CrossRefGoogle Scholar
  4. Berkyova S, Munnecke A (2010) “Calcispheres” as a source of lime mud and peloids–evidence from the early Middle Devonian of the Prague Basin, the Czech Republic. Bull Geosci 85:585–602CrossRefGoogle Scholar
  5. Brenchley PJ, Carden GA, Hints L, Kaljo D, Marshall JD, Martma T, Meidla T, Nõlvak J (2003) High-resolution stable isotope stratigraphy of Upper Ordovician sequences: constraints on the timing of bioevents and environmental changes associated with mass extinction and glaciation. Geolo Soc Am Bull 115:89–104CrossRefGoogle Scholar
  6. Calner M, Lehnert O, Nõlvak J (2010) Palaeokarst evidence for widespread regression and subaerial exposure in the middle Katian (Upper Ordovician) of Baltoscandia: significance for global climate. Palaeogeogr Palaeoclimatol Palaeoecol 296:235–247CrossRefGoogle Scholar
  7. Dronov A, Rozhnov S (2007) Climatic changes in the Baltoscandian Basin during the Ordovician: sedimentological and palaeontological aspects. Acta Palaeontol Sin 46(Supplement):108–113Google Scholar
  8. Ebbestad JOR, Högström AES (2007) Ordovician of the Siljan District, Sweden. WOGOGOB 2007, 9th meeting of the Working Group on Ordovician geology of Baltoscandia, field guide and abstracts vol 128, pp 52–58Google Scholar
  9. Freile D, Milliman JD, Hillis L (1995) Leeward bank margin Halimeda meadows and draperies and their sedimentary importance on the western Great Bahama Bank slope. Coral Reefs 14:27–33CrossRefGoogle Scholar
  10. Granier B (2012) The contribution of calcareous green algae to the production of limestones: a review. Geodiversitas 34:35–60CrossRefGoogle Scholar
  11. Harris MT, Sheehan PM, Ainsaar L, Hints L, Männik P, Nõlvak J, Rubel J (2004) Upper Ordovician sequences of western Estonia. Palaeogeogr Palaeoclimatol Palaeoecol 210:135–148CrossRefGoogle Scholar
  12. Hints L, Meidla T (1997) Keila Stage, Oandu Stage, Rakvere Stage. In: Raukas A, Teedumäe A (eds) Geology and mineral resources of Estonia. Estonian Academy Publishers, Tallinn, pp 174–180Google Scholar
  13. Hints L, Oraspõld A, Nõlvak J (2005) The Pirgu Regional Stage (Upper Ordovician) in the East Baltic: lithostratigraphy, biozonation and correlation. Proceedings of the Estonian Academy of Sciences, Geology vol 54, pp 225–259Google Scholar
  14. Hints L, Paškevičius J, Martma T, Männik P, Nõlvak J (2016) Upper Sandbian–lower Katian bio-and chemostratigraphy in the Pajevonys-13 core section, Lithuania. Est J Earth Sci 65(2):85–97CrossRefGoogle Scholar
  15. Hucke K, Voigt E (1967) Einführung in die Geschiebeforschung (Sedimentärgeschiebe). Nederlandse Geologische Vereniging, OldenzaalGoogle Scholar
  16. Jaanusson V (1976) Faunal dynamics in the Middle Ordovician (Viruan) of Baltoscandia. The Ordovician system: Proceedings of the Palaeontological Association, Symposium, Birmingham, September 1974, pp 301–326Google Scholar
  17. Jaanusson V (1982) Introduction to the Ordovician of Sweden. IV International Symposium on the Ordovician System, Field Exkursion Guide pp 1–9Google Scholar
  18. Jaanusson V, Martna J (1948) A section from the Upper Chasmops Series to the Lower Tretaspis Series at Fjäcka rivulet in the Siljan area, Dalarne. Bulletin of the Geological Institution of the University of Uppsala vol 32, pp 184–193Google Scholar
  19. Jux U (1966) Palaeoporella im Boda-Kalk von Dalarne. Palaeontogr B 118:153–165Google Scholar
  20. Kaljo D (1961) Some additional data on the study of Ordovician streptelasmids in Estonia. ENSV Teaduste Akadeemia Geoloogia Instituudi Uurimused vol VI 6, pp 51–67Google Scholar
  21. Kaljo D (2001) Carbon isotope stratigraphy in the latest Ordovician of Estonia. Chem Geol 175:49–59CrossRefGoogle Scholar
  22. Kaljo D, Hints L, Martma T, Nõlvak J (2017) A multiproxy study of the Puhmu core section (Estonia, Upper Ordovician): consequences for stratigraphy and environmental interpretation. Est J Earth Sci 66:77–92CrossRefGoogle Scholar
  23. Kaźmierczak J, Kremer B (2005) Early post-mortem calcified Devonian acritarchs as a source of calcispheric structures. Facies 51:554–565CrossRefGoogle Scholar
  24. Klaamann ER (1966) Inkommunikatnye tabulaty Estonii. Essti NSV Teaduste Akadeemia Geoloogia Instituut, TallinnGoogle Scholar
  25. Kõrts A, Einasto R, Männil R, Radionova E (1990) Calcareous algae. In: Kaljo D, Nestor H (eds) Field meeting 1990. An Excusrion Guidebook. Estonian Academy of Science, Tallinn, pp 97–100Google Scholar
  26. Kozlowski R, Kazmierczak J (1968) On two Ordovician calcareous algae. Acta Palaeontol Polonica 8:325–346Google Scholar
  27. Kröger B, Ebbestad JOR, Lehnert O (2016a) Accretionary mechanisms and temporal sequence of formation of the Boda Limestone mud-mounds (Upper Ordovician), Siljan District, Sweden. J Sediment Res 86:363–379CrossRefGoogle Scholar
  28. Kröger B, Hints L, Lehnert O (2016b) Ordovician reef and mound evolution: the Baltoscandian picture. Geol Mag 154:683–706CrossRefGoogle Scholar
  29. Lasemi Z, Sandberg PA (1984) Transformation of aragonite-dominated lime muds to microcrystalline limestones. Geology 12:420–423CrossRefGoogle Scholar
  30. Männil R (1958) Zur Stratigraphie der oberordovizischen Nabala-Stufe (FIa) in Estland. Eesti NSV Teaduste Akadeemia Geoloogia Instituudi Uurimused II vol 2 pp 3–17Google Scholar
  31. Männil R (1966) Istoria razvitiya Baltiyskogo bassena v ordovike. Eesti NSV Teaduste Akadeemia Geoloogia Instituudi, Tallinn, pp 1–201Google Scholar
  32. Marszalek DS (1975) Calcisphere ultrastructure and skeletal aragonite from the alga Acetabularia antillana. J Sediment Res 45:266–271CrossRefGoogle Scholar
  33. Martna J (1955) Studies on the Macrourus and Slandrom Formations I Shell Fragment Frequencies of the Macrourus Formation and Adjacent Strata at Fjäcka, Gräsgård, and File Haidar. Geol Föeningen i Stockh Förhandlingar 77:229–256CrossRefGoogle Scholar
  34. Merrill GK (1980) Ordovician conodonts from the Åland Islands, Finland. Geol Föreningen i Stockh Förhandlingar 101:329–341CrossRefGoogle Scholar
  35. Minoura N, Chitoku T (1979) Calcareous nannoplankton and problematic microorganisms found in the Late Palaeozonic Limestones. Journal of the Fac Sci 19(1–2):199–212 (Hokkaido University. Series 4, Geology and mineralogy) Google Scholar
  36. Munnecke A, Servais T (2008) Palaeozoic calcareous plankton: evidence from the Silurian of Gotland. Lethaia 41:185–194CrossRefGoogle Scholar
  37. Munnecke A, Westphal H, Reijmer JJG, Samtleben C (1997) Microspar development during early marine burial diagenesis: a comparison of Pliocene carbonates from the Bahamas with Silurian limestones from Gotland (Sweden). Sedimentology 44:977–990CrossRefGoogle Scholar
  38. Munnecke A, Samtleben C, Servais T, Vachard D (1999) Sem-observation of calcareous micro-and nannofossils incertae sedis from the Silurian of Gotland, Sweden: preliminary results. Geobios 32:307–314CrossRefGoogle Scholar
  39. Munnecke A, Servais T, Vachard D (2000) A new family of Calcareous microfossils from the Silurian of Gotland, Sweden. Palaeontology 43:1153–1172CrossRefGoogle Scholar
  40. Nestor H (1964) Stromatoporoidei ordovika i llandoveri Estonii. Trudy Instituta geologii AN ESSR pp 1–112Google Scholar
  41. Nestor H, Einasto R (1997) Ordovician and Silurian carbonate sedimentation basin. In: Raukas A, Teedumäe A (eds) Geology and mineral resources of Estonia. Estonian Academy Publishers, Tallinn, pp 192–204Google Scholar
  42. Nõlvak J (1989) Results of quantitative stratigraphic correlation of the Upper Ordovician in the Baltic: chitinozoans. In: Oleynikov A, Rubel M (eds) Quantitative stratigraphy—retrospective evaluation and future development. Estonian Academy of Science, Tallinn, pp 139–154Google Scholar
  43. Nõlvak J, Bauert G (2006) Kerguta (565) drill core, Distribution of Ordovician chitinozoans. Est Geolo Sect Bull 7:9–11Google Scholar
  44. Nõlvak JAAK, Meidla T, Uutela A (1995) Microfossils in the Ordovician erratic boulders from southwestern Finland. Bull Geol Soc Finl 67:3–26CrossRefGoogle Scholar
  45. Oraspõld A (1982) Lithological characterization of the boundary beds of the Vormsi and Pirgu stages in Central Estonia. Töid geoloogia alalt, VIII. Aluspõhja kivimite litostratigraafia ja mineraloogia 527:75–82Google Scholar
  46. Oraspõld A, Kala E (1982) Lithology of the Vormsi Stage in Estonia. Töid geoloogia alalt, VIII. Aluspõhja kivimite litostratigraafia ja mineraloogia 257:51–74Google Scholar
  47. Põldvere A (2001) Valga (10) Drill Core. Est Geol Sect Bull 3:1–50Google Scholar
  48. Põlma L (1972) Skeletal debris content and composition in the sediments of the northern facial belt of the East Baltic Ordovician (Rapla boring). Proceedings of the Academy of Sciences of the Estonian SSR. Chemistry and Geology vol 21 pp 326–332Google Scholar
  49. Põlma L (1973) Lithological differences between two structural-facial belts of the East Baltic Ordovician. Proceedings of the Academy of Sciences of the Estonian SSR. Chemistry and Geology vol 22 pp 240–247Google Scholar
  50. Põlma L (1982) Comparative lithology of the ordovician carbonate rocks in the Northern and Middle East Baltic. Valgus, TallinnGoogle Scholar
  51. Preobrazhensky B, Klaamann E (1975) Relations between the genera Sarcinula, Calapoecia and Lyopora (Tabulata). Proceedings of the Academy of Sciences of the Estonian SSR. Chemistry and Geology vol 24 pp 130–136Google Scholar
  52. Raukas A, Teedumäe A (eds) (1997) Geology and mineral resources of Estonia. Estonian Academy Publishers, TallinnGoogle Scholar
  53. Servais T, Munnecke A, Versteegh GJM (2009) Silurian calcispheres (Calcitarcha) of Gotland (Sweden): comparisons with calcareous dinoflagellates. C R Palevol 8:527–534CrossRefGoogle Scholar
  54. Shen Y, Neuweiler F (2016) Taphocoenoses and diversification patterns of calcimicrobes and calcareous algae, Ordovician, Tarim Basin, China. Can J Earth Sci 53:702–711CrossRefGoogle Scholar
  55. Sliaupa S, Fokin P, Lazauskiene J, Stephenson RA (2006) The Vendian-Early Palaeozoic sedimentary basins of the East European Craton. Geological Society, London, Memoirs vol 32 pp 449–462CrossRefGoogle Scholar
  56. Spjeldnæs N, Nitecki MH (1994) Baltic Ordovician lithographic limestones. Geobios 27(Supplement 1):267–273CrossRefGoogle Scholar
  57. Stolley E (1896) Über gesteinsbildende Algen und die Mitwirkung solcher bei der Bildung der skandinavisch-baltischen Silurablagerungen. Naturwissenschaftliche Wochenschrift 11:173–178Google Scholar
  58. Stolley E (1897) Die silurische Algenfacies und ihre Verbreitung im skandinavisch-baltischen Silurgebiet. Schriften des Naturwissenschaftlichen Vereins Schleswig-Holstein 11:109–148Google Scholar
  59. Thorslund P (1960) The Cambro-Silurian of Sweden. Sveriges Geologiska Undersökning B 16:69–110Google Scholar
  60. Tynni R (1982) On Paleozoic microfossils in clastic dykes in the Åland Islands and in the core samples of Lumparn. Geol Surv Finl Bull 317:35–114Google Scholar
  61. Uutela A (1989) Age and dispersal of sedimentary erratics on the coast of Finland. Geol Surv Finl Bull 349:1–100Google Scholar
  62. Versteegh GJM, Servais T, Streng M, Munnecke A, Vachard D (2009) A discussion and proposal concerning the use of the term calcispheres. Palaeontology 52:343–348CrossRefGoogle Scholar
  63. Vingisaar P (1971) A microlithological study of the Ordovician limestones from the Haapsalu boring. Proceedings of the Academy of Sciences of the Estonian SSR. Chemistry and Geology vol 20 pp 54–59Google Scholar
  64. Warburg E (1910) Geological description of Nittsjö and its environs in Dalarne. GFF 32:425–450Google Scholar
  65. Wiman C (1893) Über das Silurgebiet des Bottnischen Meeres, vol 1. Bulletin of the Geological Institute University, Uppsala, pp 1–11Google Scholar
  66. Winterhalter B (1972) On the geology of the Bothnian Sea, an epeiric sea that has undergone Pleistocene glaciation. Geol Surv Finnl Bull 258:1–66Google Scholar
  67. Zhang Y, Li Y, Munnecke A (2014) Late Ordovician microbial reefs in the Lianglitag Formation (Bachu, Tarim, NW China). Facies 60:663–684CrossRefGoogle Scholar
  68. Zheng L, Bao H, Wu Y, Sun L, Jiang H, Ren J, Huang Z, Liu L (2018) Distinguishing coral reef facies from coral-bearing open platform facies: examples from Ordovician Ordos Basin, Northwest China. Palaeogeogr Palaeoclimatol Palaeoecol 495:72–86CrossRefGoogle Scholar

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Authors and Affiliations

  1. 1.Finnish Museum of Natural HistoryUniversity of HelsinkiHelsinkiFinland
  2. 2.School of Resources and Environmental EngineeringHefei University of TechnologyHefeiChina
  3. 3.Geozentrum Nordbayern, Fachgruppe PaläoumweltFriedrich-Alexander Universität Erlangen-NürnbergErlangenGermany

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