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[delta][sup.13]C chemostratigraphy of the Middle and Upper Ordovician succession in the Tartu-453 drillcore, southern Estonia, and the significance of the HICE.

INTRODUCTION AND GEOLOGICAL BACKGROUND

The Baltoscandian region is a well-known key area for global Ordovician biostratigraphic and chemostratigraphic research. Extensive stable carbon isotope chemostratigraphic studies of the Baltoscandian Ordovician-Silurian carbonate succession conducted in the last decade have revealed a series of positive [delta][sup.13]C isotope excursions (ICE) that have shown a great potential for both intrabasinal (in the Palaeobaltic basin) and global stratigraphic correlations.

The log/description of the Tartu-453 drillcore with biostratigraphic data of some microfossil groups on certain stratigraphic units (chitinozoans: Lasnamagi to Porkuni regional stages (RSs); conodonts: Volkhov to Kunda and Lasnamagi to Keila RSs; ostracods: Volkhov to Kunda and Keila to Pirgu RSs) was published by the Geological Survey of Estonia (Poldvere 1998). The purpose of this paper is to describe the Ordovician [delta][sup.13]C chemostratigraphy in that core and to assess the relationships with coeval successions in Baltoscandia and elsewhere. Particular attention is drawn to the significance of the Hirnantian [delta][sup.13]C excursion (HICE) in establishing the Ordovician-Silurian boundary in the East Baltic area.

The 431 m deep Tartu-453 borehole that records Devonian-Cambrian strata was drilled in 1992 as a groundwater well in the southern suburb of the town of Tartu, southern Estonia. The published 151 m thick Ordovician succession (depth range 230.4-381.0 m) is mostly represented by variably argillaceous limestones of the Volkhov RS (Dapingian) to the Porkuni RS (Hirnantian). The Ordovician carbonate succession in Tartu was deposited on the area separating the wide, inner ramp or shelf (North Estonian Confacies Belt) from the deep outer ramp or basin known as the Livonian Tongue (Nestor & Einasto 1997, fig. 1). The depositional environment in the entire Baltic area evolved from temperate carbonate ramp in Dapingian-Sandbian time to the tropical carbonate shelf in Katian-Hirnantian time (Nestor & Einasto 1997).

MATERIALS AND METHODS

The [delta][sup.13]C isotopic data were obtained from 289 samples of the Billingen to Juuru RSs, using a Thermo Delta V Advance mass spectrometer at the Department of Geology of the University of Tartu. The [delta][sup.13]C values are reported in per mil relative to Vienna Pee Dee belemnite standard and the reproducibility was better than [+ or -] 0.1 [per thousand] (1 [delta]). Additionally, 33 analyses from an earlier study by Ainsaar et al. (1999; interval 292-307.3 m) were included here. The Tartu-453 drillcore is housed at the Department of Geology, University of Tartu.

[delta][sup.13]C CHEMOSTRATIGRAPHY OF THE TARTU-453 DRILLCORE

Based on the [delta][sup.13]C isotope data, a continuous Ordovician carbon isotope record was created, ranging from the Floian to the end of the Hirnantian of southern Estonia. Five positive [delta][sup.13]C excursions were recognized with certainty in the Ordovician of the Tartu-453 drillcore succession (Fig. 1). Most of these positive [delta][sup.13]C excursions clearly correspond to excursions established by Ainsaar et al. (2010) on the Baltoscandian composite [delta][sup.13]C curve, except for the Paroveja and Rakvere ICEs which are not so obvious in the Tartu-453 section. Besides the positive [delta][sup.13]C excursions, a conspicuous negative excursion, the Lower Sandbian NICE (LSNICE), was recorded in the Ordovician succession.

The Middle Darriwilian excursion (MDICE) is a well-known [delta][sup.13]C excursion which has by now been reported from various palaeocontinents (see a review in Calner et al. 2014). It was initially recognized in the core sections of the East Baltic area by Ainsaar et al. (2004). In the Tartu-453 drillcore, the MDICE is characterized by a broad positive shift with a considerable temporal extent--spanning from the Kunda to Lasnamagi ages. The protracted [delta][sup.13]C excursion starts around 0.5[per thousand] values in a highly condensed succession of red-coloured limestones with numerous hardgrounds, peaking around 1.9[per thousand] values in red-coloured limestones of Aseri age and then declining in greyish to greenish limestones of Lasnamagi age. The exact termination of the MDICE is not obvious as there is a continuous declining trend of [delta][sup.13]C values through the Lasnamagi, Uhaku and Kukruse RSs. Here we have chosen the [delta][sup.13]C value 0.5[per thousand] as a baseline value for the MDICE, which marks the end of the MDICE about 1 m underneath the Uhaku-Kukruse RSs boundary. The MDICE is well represented in several drillcore sections of the East Baltic (e.g. Kerguta-565, Mehikoorma-421, Mannamaa F-367, Ruhnu-500, Jurmala R-1, Viki; for reviews of the MDICE see Kaljo et al. 2007; Ainsaar et al. 2010; Hints et al. 2014) as well as in Swedish sections on Oland (Tingskullen drillcore: Calner et al. 2014) and in Dalarna (Kargarde section: Ainsaar et al. 2010). However, there are also densely-sampled sections in Estonia where the MDICE does not show up (e.g. Uuga cliff section at Cape Pakri, NW Estonia: fig. 2 in Tammekand et al. 2010).

The Lower Sandbian NICE (LSNICE) exhibits the most negative [delta][sup.13]C values for the whole Ordovician succession of the Tartu-453 drillcore, reaching -0.49[per thousand] in the topmost beds of the Kukruse RS. The exact temporal extent of the LSNICE is hard to determine and needs further investigations. We have tentatively set the baseline values for the LSNICE at 0[per thousand] in the Tartu-453 drillcore, resulting in the late Kukruse age for it. The LSNICE is designated as the 'upper Kukruse low' by Kaljo et al. (2007) in the Valga-10, Mehikoorma-421 and Kerguta-565 drillcore sections, although its exact temporal extent has not been shown. A strikingly similar [delta][sup.13]C curve for the MDICE and LSNICE, with the lowest [delta][sup.13]C values for the whole Ordovician succession recorded in the LSNICE, was also reported from the Ruhnu-500 drillcore (Ainsaar et al. 2004, fig. 1). In Sweden, the LSNICE most probably occurs within the Dalby Limestone in the Gullhogen quarry section, Vastergotland (Meidla et al. 2004, fig. 1) and this NICE is only barely observable (max. negative shift about -0.5[per thousand] from background values) in the Borenshult drillcore section, Ostergotland (Bergstrom et al. 2012, fig. 5). A remarkable decrease in [delta][sup.13]C values to almost -4[per thousand], succeeding the MDICE peak around +1[per thousand], was recorded by Leslie et al. (2011, fig. 3) in the Clear Spring, Maryland section along Interstate-70. This conspicuous negative [delta][sup.13]C excursion in the Clear Spring section could be regarded as LSNICE, however, the conodont data from the Appalachian section imply a somewhat older age (the top of the Cahabagnathus friendsvillensis Zone) compared to conodont data from the Tartu-453 core (the lowest [delta][sup.13]C values were recorded in the topmost Kukruse beds, immediately below the base of the Baltoniodus gerdae Subzone; S. Stouge unpublished data).

The second largest [delta][sup.13]C isotope excursion known in the Ordovician, the Guttenberg ICE (GICE), is recorded in the Tartu-453 drillcore as a distinct asymmetric peak in the highly argillaceous to silty limestones of late Keila to early Oandu age. The GICE is characterized by a continuous increase in [delta][sup.13]C values (from ca 0.5[per thousand] to a max value of 2.20[per thousand]) in late Keila limestones, followed by a sharp decline to 1.36[per thousand] at about the Keila and Oandu RSs boundary. This sharp turnover level marks a major change in chitinozoan faunas (J. Nolvak pers. comm. 2014) and an increased influx of fine silt-sized siliciclastic material into the sedimentary basin during the Oandu age (Variku Formation: Ainsaar & Meidla 2001). The middle part of the GICE shows slightly fluctuating [delta][sup.13]C values around 1.4[per thousand] and the characteristics of the GICE falling limb are unknown due to missing core between 288.45 and 292.5 m.

Based on the [delta][sup.13]C chemostratigraphy reviews in the Baltic area by Kaljo et al. (2007) and Ainsaar et al. (2010), the GICE displays a well-developed positive peak in the drillcore sections derived from southern Estonia and Latvia (Mehikoorma-421, Valga-10, Ruhnu-500, Viljandi, Jurmala R-1). However, this excursion is not that clear or even might be missing in central and western Estonia (Kerguta-565, Rapla, Mannamaa F-367 drillcore sections). It should be noted that the GICE curves both in the Tartu-453 and Mehikoorma-421 sections look remarkably similar to each other.

Elsewhere in Baltoscandia, the pronounced GICE curves have been reported from Norway--in the Frognerkilen Formation, Oslo-Asker area (Bergstrom et al. 2011, fig. 4) and in the [SIGMA] Mjosa Formation, Lake Mjosa area (Bergstrom et al. 2011, fig. 3). In Sweden, the GICE was recently firmly recorded in the Freberga Formation of the Borenshult drillcore, Ostergotland (Bergstrom et al. 2012, fig. 6). A comprehensive overview of the GICE occurrences in North America is given by Bergstrom (2010a).

The Middle Katian succession, comprising the Rakvere, Nabala and Vormsi RSs, is highly condensed and only 8.4 m thick in the Tartu-453 drillcore section. Thus, the Rakvere ICE cannot be reliably identified, however, the Saunja ICE (with an almost 1[per thousand] positive shift) clearly stands out on the isotope curve at the boundary interval of the Nabala and Vormsi RSs. The Saunja ICE in the Mehikoorma-421 drillcore in SE Estonia is correlated by Bergstrom et al. (2010b, fig. 7) with the Waynesville ICE--the latter is observed in several Katian sections of the US Midcontinent. The Saunja ICE peak is usually easily recognizable on [delta][sup.13]C curves of Estonian drillcores (Kaljo et al. 2007, fig. 3; Ainsaar et al. 2010, figs 3, 4; Hints et al. 2014, fig. 2) as well as in the Jurmala R-1 drillcore, Latvia (Ainsaar et al. 2004, fig. 1), but it seems to be missing due to the gap in sedimentation in the Borenshult drillcore section from Ostergotland, Sweden (Bergstrom et al. 2012, fig. 3).

Two small positive [delta][sup.13]C shifts, in a range of about 0.5-0.8[per thousand], have been identified in the Jonstorp Formation of the Tartu-453 drillcore. The lower ICE is considered on the grounds of its lithostratigraphic position to correspond to the Moe ICE. However, it should be mentioned that we lack any biostratigraphic age evidence for both isotope excursions in the Jonstorp Formation because chitinozoans were destroyed by oxidation in red-coloured limestones. Owing to this uncertainty, we have not assigned a name to the upper ICE in the Jonstorp Formation. There seems to occur an interval with somewhat elevated [delta][sup.13]C data (shift from background values is < 0.5[per thousand]) in the boundary beds of the Pirgu and Porkuni RSs. Most probably this small [delta][sup.13]C shift could represent the Paroveja ICE proposed by Ainsaar et al. (2010, fig. 7).

The Hirnantian ICE exhibits the most spectacular positive [delta][sup.13]C excursion in the Ordovician succession of the Tartu-453 drillcore with the peak value of +4.33[per thousand] (this shift is over 3[per thousand] from the baseline value of ca 1[per thousand]). Instead of a commonly observed relatively uniform curve, the Hirnantian ICE displays a rather unusual twin-peaked [delta][sup.13]C curve in the Tartu-453 section. A similar, well-developed twin-peaked Hirnantian ICE is also recorded in the NACP drillcore section of Anticosti Island, Canada (Desrochers et al. 2010, fig. 4). The overall shape of the [delta][sup.13]C excursion in the Tartu-453 drillcore is clearly asymmetric, characterized by a fast rise in [delta][sup.13]C values on the lower limb and by a considerably slower decline in [delta][sup.13]C values on the upper limb. The onset of the Hirnantian ICE is recorded at a depth of about 235 m in the argillaceous limestones of the Halliku Formation (Late Porkuni age) and it terminates at a depth of about 220 m in the marlstones of the Ohne Formation (Juuru age).

THE ORDOVICIAN-SILURIAN BOUNDARY IN THE TARTU-453 DRILLCORE

The Ordovician-Silurian boundary is marked by the FAD of Akidograptus ascencus and Parakidograptus acuminatus at the GSSP site for the base of the Silurian System in the Dob's Linn section of Scotland (Williams, 1988). These biostratigraphically diagnostic graptolites, however, are not known in the Baltic area. The base of the Silurian System in Estonia is traditionally drawn at the base of the Juuru RS (Nestor 1997). Based on the [delta][sup.13]C chemostratigraphic studies of the Ordovician-Silurian boundary beds in central Estonia, Ainsaar et al. (2011) concluded that the lowermost strata of the Juuru RS (Koigi Member) may be Ordovician rather than Silurian in age. Hints et al. (2014, fig. 3) reached the same conclusion on the grounds of carbon and sulphur isotope studies of the Hirnantian ICE in the Viki drillcore, Saaremaa Island.

The uniqueness of the HICE in the Tartu-453 drillcore section, compared to the other sections (Kaljo et al. 2008; Ainsaar et al. 2010; Hints et al. 2014), lies in the fact that the HICE extends substantially upwards (about 10 m) from the Porkuni-Juuru RSs boundary, into the marlstones of the Ohne Formation. In their recent overview on the Hirnantian chemostratigraphy in Sweden and elsewhere Bergstrom et al. (2014, fig. 2) have shown that the diagnostic graptolites for the Ordovician-Silurian boundary were first found even a few metres above the termination of the HICE. This evidence allows us to tentatively draw the Ordovician-Silurian boundary in the Tartu-453 drillcore section at a depth of 218.8 m, which marks the change in lithologies in the Ohne Formation at the level of a limonitized dicontinuity surface.

CONCLUSIONS

Based on the high-resolution [delta][sup.13]C chemostratigraphic study of the Ordovician succession in the Tartu-453 drillcore, we firmly identified five positive excursions and one negative excursion, which correlate well with other chemostratigraphically studied sections in Baltoscandia. The well-expressed HICE extends about 10 m from the traditional Ordovician-Silurian boundary (between the Porkuni and Juuru RSs) into the Juuru RS. According to the recent [delta][sup.13]C chemostratigraphic studies in Sweden, containing diagnostic graptolites for establishing the base of the Silurian System, it seems plausible to raise the Ordovician-Silurian boundary in the Tartu-453 drillcore section 11.6 m upwards into the Juuru RS and to draw it at a level of a limonitized discontinuity surface at a depth of 218.8 m (Fig. 2).

doi: 10.3176/earth.2014.18

Acknowledgements. We thank the reviewers S. Young and K. Histon for valuable comments on our manuscript. The study was supported by the Estonian Research Council grant IUT20-34. This paper is a contribution to IGCP Project 591.

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Heikki Bauert (a), Leho Ainsaar (b), Kairi Poldsaar (b) and Siim Sepp (b)

(a) Institute of Geology at Tallinn University of Technology, Ehitajate tee 5, 19086 Tallinn, Estonia; heikki.bauert@ttu.ee

(b) Department of Geology, University of Tartu, Ravila 14A, 50411 Tartu, Estonia; leho.ainsaar@ut.ee, kairi.poldsaar@ut.ee, siim.sepp@ut.ee

Received 2 July 2014, accepted 16 October 2014
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Author:Bauert, Heikki; Ainsaar, Leho; Poldsaar, Kairi; Sepp, Siim
Publication:Estonian Journal of Earth Sciences
Article Type:Report
Geographic Code:4EXES
Date:Dec 1, 2014
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