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Correlation of Telychian sections from shallow to deep sea facies in Estonia and Latvia based on the sanidine composition of bentonites/Eesti ja Lati madal- ja suvamere faatsieste Telychi labiloigete korrelatsioon bentoniitide sanidiini koostise alusel.

INTRODUCTION

The idea that volcanic ash beds in sedimentary sections can be used as perfect time markers for correlations was proposed long ago (e.g. Spjeldnaes 1959). Although now tephrochronology is used successfully in Quaternary geology and archaeology, identification of coeval ash beds in the Palaeozoic rocks appears to be more complicated. The reason is that the ash consists mainly of unstable amorphous material which recrystallizes easily in exogenic environments. As a result, various clay minerals and other authigenic silicates form (Ross & Shannon 1926; Grim & Guven 1978; Altaner et al. 1984; Caballero et al. 1992; Huff et al. 1996; Kiipli et al. 1997). Therefore, main chemical components and minerals cannot be used directly for correlation of ancient volcanic beds. Some elements exhibit low mobility in exogenic environments and can be used for restoring source magma in altered volcanic rocks (Winchester & Floyd 1977). Correlation on the basis of immobile trace elements has been successfully used in many works (Huff & Kolata 1989; Batchelor & Jeppsson 1994; Bergstrom et al. 1995; Kiipli et al. 2001). Attempts to correlate ash beds from different facies may still fail due to the variable degree of residual enrichment of material with immobile elements in different environments. Also, no element can be strictly defined as immobile--even the low mobility elements can move to some extent. The study of trace magmatic minerals allows us to overcome these problems and to identify the bentonites. In the present study we used the composition of magmatic sanidine to recognize coeval volcanic beds in different sections.

TELYCHIAN SECTIONS IN ESTONIA AND LATVIA

The Llandovery-Wenlock boundary interval in Estonia, corresponding to a relatively high sea level period (Johnson et al. 1991), is represented by up to 95 m thick claystones and marlstones lying between nodular limestones (Rumba Formation) and reef and lagoonal dolostones (Jaagarahu and Muhu formations). In these rocks the Adavere and Jaani regional stages are distinguished (Fig. 1). The former has been correlated with the Upper Llandovery and the latter with the Lower Wenlock (Aaloe 1960; Kaljo 1962; Nestor 1997). In a relatively homogeneous claystone-marlstone sequence the boundary of these regional stages is often placed at different levels in different sections, and even in one section. For example, in the Viki core this boundary has been established at the following depths: 153.8 m (Jeppsson & Mannik 1993), 135 m (Nestor 1994, fig. 14), 145.8 m (Nestor 1994, table 4 combined with fig. 3; Nestor 1997, fig. 65), 133.5 m (Nestor 1997, fig. 69). The cause of such indistinctness is different palaeontological or lithological criteria used by different authors. The original criterion for this boundary used by Aaloe (1960) was the uppermost one of the volcanic ash beds in the interval of their frequent occurrence. In the Viki core, it lies at 145.7 m, close to the beginning of the Pterospathodus amorphognathoides amorphognathoides conodont Zone (Kiipli et al. 2001).

In the Ohesaare core, represented by the graptolite facies, the Llandovery-Wenlock boundary was placed at the volcanic ash bed at a depth of 345.8 m. Cyrtograptus murchisoni occurs 0.7 m above this ash bed (Kaljo 1962). Later, the lowermost findings of this graptolite have been identified as Cyrtograptus centrifugus (Loydell et al. 1998). This level lies in the middle of the Pterospathodus amorphognathoides amorphognathoides Zone (Loydell et al. 1998, and correlation of bentonites in the present study), therefore clearly higher than the Adavere-Jaani boundary in the northern, shallower palaeoshelf sections.

In Latvia, Telychian sections are represented by red, grey, and variegated claystones above dark organic-rich argillites of the Dobele Formation. The upper boundary is not marked lithologically and can be established only by the appearance of Wenlock graptolites.

MATERIAL AND METHODS

A total of 130 samples from 12 cores were studied from volcanic beds with a thickness between 0.2 and 25 cm (Fig. 2). The same samples from six cores, representing relatively shallow palaeosea facies, were formerly used in Kiipli et al. (2001) for correlating sections on the basis of immobile trace elements. Two sections of the present study (Aizpute and Ohesaare) are located in the deep shelf facies and one (Kaugatuma) lies near the boundary between the deep and shallow shelf facies. Mineralogy of volcanic beds is different from that of host rock. In the volcanic beds illite-smectite, kaolinite, and potassium feldspar (authigenic K-sanidine) dominate. The host rock is composed mainly of illite, potassium feldspar (orthoclase), and terrigenous quartz. Coarse fractions contain euhedral and broken magmatic quartz, biotite, and K-Na sanidine. The estimated content of magmatic phenocrysts was 1-10% of the bulk sediment. According to Kastner (1971) and Kastner & Siever (1979), sedimentary authigenic feldspars have a pure end member composition. Sanidine formation in magmatic processes, on the contrary, is characterized by a variable K to Na ratio in solid solution. Therefore, for correlation purposes we studied magmatic K-Na sanidine. The presence of sanidine of variable composition in Silurian bentonites of Gotland was established by Snall (1977), but was not used for correlation of sections.

[FIGURE 2 OMITTED]

Sample preparation

About 1-5 g of a sample was suspended ultrasonically in distilled water and after 20 s the clay suspension was poured out. If kaolinite was still present in coarse fraction, it was disperged ultrasonically in 20% KOH solution and poured out. The residue was treated by hot 2N HCl solution, to clean the sample of hematite, calcite, apatite, and products of pyrite oxidation (gypsum, Fe-sulphates). The cleaned coarse fraction still contained, besides magmatic minerals (K-Na sanidine, quartz, biotite, zircon), also authigenic K-sanidine, pyrite or chalcopyrite. In a few samples barite occurred. The content of these minerals varied largely. Sulphides were removed by nitric acid. If the sample was large enough, the 0.04-0.1 mm and 0.1-0.25 mm fractions were separated by sieving. Pyroclastic grains larger than 0.25 mm were not found. The 0.1-0.25 mm fraction was present only in some beds, 0.04-0.1 mm fraction was established in all beds and therefore suits best for correlation studies. The fine (<0.04 mm) fraction is not suitable for the study of magmatic sanidine due to a higher content of authigenic K-sanidine, which complicates also analysis of coarser fractions. In the case of feldspathites (volcanogenic interbeds consisting mostly of authigenic potassium feldspar), it is impossible to achieve the concentration of magmatic phenocrysts sufficient for detailed study. For XRD analysis the sample was ground by hand in an agate mortar and a slurry mount was prepared using ethyl alcohol and glass slide.

Measurements

Measurements were performed on the HZG-4 diffractometer (Freiberger Prazisionmechanik) using Fe-filtered Co-radiation. All samples were routinely scanned from 5 to 45[degrees] 2[theta] before any treatment in order to check their volcanic origin and estimate the mineralogical composition. From the separated fraction the 20 [bar.1] reflection of sanidine was measured with maximum accuracy. An angle range from 23.5 to 26.0[degrees] 2[theta] was scanned with the step size 0.01[degrees] 2[theta]; the measuring time was 15 s per point. This range includes the 100 reflection of quartz, the 20 [bar.1] reflection of various feldspar phases, and also 4.18 and 4.13 [Angstrom] reflections of kaolinite. Therefore, removal of kaolinite from the sample before measurements is essential.

Calculation of the sanidine composition

A curve-fitting programme performed in MathCad 2000 was applied for calculating the exact peak position, half-width, and intensity. The measured X-ray pattern was fitted with convolution of mineral reflection and instrumental profile. The profile of quartz heated for 7 h at 800[degrees]C was used as instrumental profile. The peak position, half-width, and intensity were calculated for four components: quartz, K-sanidine, and two K-Na sanidines. The K-Na sanidine peak position was calculated in relation to quartz or K-sanidine, depending on which of these minerals dominated in a specimen. The angle distance between quartz and K-sanidine reflections appeared to be constant, pointing to the stable composition of both minerals. Only rare traces of plagioclase were detected and therefore plagioclase reflection was not included in curve-fitting. Examples of the measured diffractograms are shown in Fig. 3.

The content of NaAl[Si.sub.3][O.sub.8] in mol% in K-Na sanidine was calculated according to Orville (1967), who established that the position of the 20 [bar.1] reflection almost linearly depends on the composition of sanidine solid solution. Fast cooling of volcanic ash avoids exsolution of feldspar and favours the preservation of magmatic sanidine; therefore calculation of the feldspar composition according to the method proposed by Orville can be estimated as accurate. In perthites, calculation of the sanidine composition on the basis of only the 20 [bar.1] reflection can lead to imprecise results because of the strain between two feldspar phases (Stewart & Wright 1974). Late recrystallization of magmatic sanidine resulting in perthite formation supposedly did not take place because the rocks have not been heated more than 50-100[degrees]C during the geological history, as indicated by the alteration index of conodonts, which varies between 1 and 2 in the Silurian and Ordovician rocks of Estonia (Mannik & Viira 1990). The precision of the analysis of the K-Na sanidine composition is [+ or -] 1% in favourable cases (low intensity of authigenic feldspar reflection, no kaolinite, high intensity of the magmatic sanidine reflection) and [+ or -] 2% in less favourable cases.

RESULTS

K-Na sanidine of various composition was found, containing 20-47 mol% NaAl[Si.sub.3][O.sub.8]. In a few bentonite samples magmatic sanidine was at the level of the detection limit. Magmatic sanidine was not found in terrigenous samples. The rest of the volcanic samples contained a measurable amount of K-Na sanidine. Two groups of samples can be distinguished: (1) The samples exhibiting a wide elevated interval in XRD spectra without a specific well distinguishable reflection. This type can be interpreted as containing a mixture of K-Na sanidine of variable composition. Correlation of this type is not certain and can be done with some probability between beds with signs allowing better identification. Twelve of the studied beds show this type of sanidine pattern. (2) The samples exhibiting well measurable reflections and allowing calculations of the K-Na sanidine composition. These beds can be found and correlated in the studied sections with a high level of probability. Twenty-three of the studied beds revealed well measurable sanidine reflections. The reflection width varied largely and in case of wide reflections the XRD pattern was transitional between two types. Commonly, even in the presence of a sharp K-Na sanidine peak, a wide elevated region in spectra was observed. Therefore, curve-fitting with three components (quartz, K-sanidine, and one K-Na sanidine) was only rarely satisfactory, but four-component fitting revealed good results in all cases (Fig. 3). Twenty-nine volcanic beds are correlated in at least two core sections; 18 of these can be identified in four or more sections. Eight volcanic beds were identified only in one section (Table 2). A total of 37 volcanic beds were established in the Telychian sequence of Estonia and Latvia. The maximum number of volcanic beds in a single section is 23 (Ohesaare). In Table 1 two formerly published numbering systems are presented (Kiipli 1998; Kiipli et al. 2001), both beginning with zero (0) which designates the bentonite well known in Estonia as "O". This bed was named Osmundsberg K-bentonite by Bergstrom et al. (1998). With only a few corrections correlations by sanidine compositions well correspond to the correlations formerly performed by trace elements (Kiipli et al. 2001). Present correlations well concord with biostratigraphy (Jeppsson & Mannik 1993; Loydell et al. 1998) but allow also some refinements in the correlation of graptolite and conodont biozones. More detailed biostratigraphical analysis is currently under preparation.

[FIGURE 3 OMITTED]

SOME PROBLEMS

Until the bed has been identified in at least two sections, its stratigraphic position cannot be considered as proved. For example, in the Mustjala core two beds, at 115.87 and 117.80 m, can be well characterized by their sanidine compositions, but in other cores beds with a similar composition have opposite succession. The bed at 115.87 m in Mustjala can be correlated with the bed at 191.95 m in Tehumardi and the bed at 117.80 m in Mustjala with the bed at 190.30 m in Tehumardi. Thus, this part of the Mustjala core is possibly not in right order in the core box or one of these beds is new in Mustjala, not found in other cores. Considering graphic correlations based on currently available information, we chose a preliminary correlation as presented in Tables 1 and 2.

[FIGURE 4 OMITTED]

Several volcanic beds of the Aizpute core with wide reflections are correlated only tentatively with other sections as their sanidine composition does not allow us to prove or refute correlations. Trace elements that helped correlation of these beds in Saaremaa have not been analysed in Aizpute. On the other hand, the number of beds with wide reflections at close stratigraphical levels is similar in Saaremaa and Aizpute (5 and 6, respectively). In Table 1 the supposed preliminary correlation is given with smaller font. The bed at 953.99 m in Aizpute, containing sanidine with a high sodium content, and the bed at 369.12 m in Ohesaare with high Nb and Zr (Kiipli & Kallaste 1996) were correlated by analogy with other beds with high Nb and Zr contents and sodium-rich sanidine (beds 2, 17, 19, 20, Kiipli 1998). Direct correlation using the same criterion is not possible as no more sample material for analyses is available from these beds.

Depths of volcanic beds above 940 m in the Aizpute section must be considered as conventional, as drilling depth records allow different interpretations in the range [+ or -] 2-3 m. Comparison with biostratigraphic analyses is possible only by using sampling markers on core boxes.

Sanidine from 370.77 m in Ohesaare shows a somewhat different diffractogram for bed 2 compared to the others. It has a characteristic sharp peak, but also a wide tail-like reflection. It was noticed in the process of the preparation of the sample that this thin bed consisted of two visually different parts. Therefore we suppose that the sample consists of a mixture of two successive eruptions (beds 2 and 3) and sediment thickness between these beds is reduced to zero in Ohesaare (0.5 m in the Viki core).

CONCLUSIONS

1. The composition of magmatic K-Na sanidine in volcanic ash beds is a valuable tool for identification of coeval beds in sections, allowing crossing the facies boundaries.

2. Correlations of volcanic ash beds of shallow shelf sections and the deep shelf Ohesaare section generally confirm but enable also some refinements of graptolite- and conodont-based correlations by Loydell et al. (1998).

3. Correlations based on many volcanic beds reveal sedimentological features (condensation of sedimentation, facies movements) difficult to establish by other methods.

ACKNOWLEDGEMENTS

We thank the referees D. Kaljo and S. Snall for useful remarks which considerably improved the manuscript. Financial support for this research was provided by the Estonian Science Foundation (grant No. 4070).

Received 22 October 2001, in revised form 23 January 2002

REFERENCES

Aaloe, A. 1960. New research into the Silurian stratigraphy of Estonia. Eesti TA Geol. Inst. Uurimused, 5, 123-141 (in Russian).

Altaner, S. P., Hower, J., Whitney, G. & Aronson, J. L. 1984. Model for K-bentonite formation: evidence from zoned K-bentonites in the disturbed belt, Montana. Geology, 12, 412-415.

Batchelor, R. A. & Jeppsson, L. 1994. Late Llandovery bentonites from Gotland, Sweden, as chemostratigraphic markers. J. Geol. Soc. London, 151, 741-746.

Bergstrom, S. M., Huff, W. D., Kolata, D. R. & Bauert, H. 1995. Nomenclature, stratigraphy, chemical fingerprinting, and areal distribution of some Middle Ordovician K-bentonites in Baltoscandia. GFF, 117, 1-13.

Bergstrom, S. M., Huff, W. D. & Kolata, D. R. 1998. The Lower Silurian Osmundsberg K-bentonite. Part I: stratigraphic position, distribution, and palaeogeographic significance. Geol. Mag., 135, 1-13.

Caballero, E., Reyes, E., Delgado, A., Huertas, F. & Linares, J. 1992. The formation of bentonite: mass balance effects. Appl. Clay Sci., 6, 265-276.

Grim, R. E. & Guven, N. 1978. Bentonites. Geology, mineralogy, properties and uses. Developments Sedimentol., 24.

Huff, W. D., & Kolata, D. R. 1989. Correlation of K-bentonite beds by chemical fingeprinting using multivariate statistics. In Quantitative Dynamic Stratigraphy (Cross, T. A., ed.), pp. 567-577. Prentice Hall.

Huff, W. D., Kolata, D. R., Bergstrom, S. M. & Zhang, Y.-S. 1996. Large-magnitude Middle Ordovician volcanic ash falls in North America and Europe: dimensions, emplacement and post emplacement characteristics. J. Volcanol. Geothermal Res., 73, 285-301.

Jeppsson, L. & Mannik, P. 1993. High resolution correlations between Gotland and Estonia near the base of the Wenlock. Terra Nova, 5, 348-358.

Johnson, M. E., Baarli, B. G., Nestor, H., Rubel, M., & Worsley, D. 1991. Eustatic sea level patterns from the Lower Silurian (Llandovery Series) of Southern Norway and Estonia. Geol. Soc. Amer. Bull., 103, 315-335.

Kaljo, D. 1962. On the boundary of the Llandoverian and Wenlockian in the East Baltic. Eesti TA Geol. Inst. Uurimused, 10, 97-113 (in Russian).

Kaljo, D., Kiipli, T. & Martma, T. 1998. Correlation of carbon isotope events and environmental cyclicity in the East Baltic Silurian. In Silurian Cycles (Landing, E. & Johnson, M. E., eds.). New York State Mus. Bull., 491, 297-312.

Kastner, M. 1971. Authigenic feldspars in carbonate rocks. Amer. Mineral., 56, 1403-1442.

Kastner, M. & Siever, R. 1979. Low temperature feldspars in sedimentary rocks. Amer. J. Sci., 279, 435-479.

Kiipli, E. & Kallaste, T. 1996. Geochemical characterization of some Estonian metabentonites. Proc. Estonian Acad. Sci. Geol., 45, 68-77.

Kiipli, T. 1998. Vulkanogeensed kihid Eesti settekivimites. In 60 aastat maeinseneride opetamist Eestis (Reinsalu, E., ed.), pp. 9-12. Tallinna Tehnikaulikool Maeinstituut, Tallinn.

Kiipli, T. & Tsegelnjuk, P. D. 2001. Rare metals in volcanic ash beds in Silurian sedimentary sections of Estonia, Ukraine and Moldova--application for correlations between regions. In Rare Metals in Ukraine--View to the Future (Galetsky, L. S., ed.), pp. 59-61. Acad. Sci. Ukraine, Kiev.

Kiipli, T., Kiipli, E. & Kallaste, T. 1997. Metabentonite composition related to sedimentary facies in the Lower Silurian of Estonia. Proc. Estonian Acad. Sci. Geol., 46, 93-104.

Kiipli, T., Mannik, P., Batchelor, R. A., Kiipli, E., Kallaste, T. & Perens, H. 2001. Correlation of Telychian (Silurian) altered volcanic ash beds in Estonia, Gotland and Norway. Norwegian J. Geol., 81, 179-193.

Loydell, D. K., Kaljo, D. & Mannik, P. 1998. Integrated biostratigraphy of the lower Silurian of the Ohesaare core, Saaremaa, Estonia. Geol. Mag., 135, 769-783.

Mannik, P. & Viira, V. 1990. Conodonts. In Field Meeting Estonia 1990. An Excursion Guidebook (Kaljo, D. & Nestor, H., eds.), pp. 84-89. Inst. Geol. Estonian Acad. Sci., Tallinn.

Nestor, H. 1997. Silurian. In Geology and Mineral Resources of Estonia (Raukas, A. & Teedumae, A., eds.), pp. 89-106. Estonian Acad. Publ., Tallinn.

Nestor, V. 1994. Early Silurian chitinozoans of Estonia and North Latvia. Academia, 4, Estonian Acad. Publ., Tallinn.

Orville, P. M. 1967. Unit cell parameters of the microcline--low-albite and the sanidine high-albite solid solution series. Amer. Mineral., 52, 55-86.

Ross, C. S. & Shannon, E. V. 1926. Minerals of bentonite and related clays and their physical properties. J. Amer. Ceramic Soc., 9, 77-96.

Spjeldnaes, N. 1959. Silurian bentonites from Gotland, Sweden. GFF, 81, 582-587.

Snall, S. 1977. Silurian and Ordovician bentonites of Gotland (Sweden). Stockholm Contrib. Geol., 31.

Stewart, D. B. & Wright, T. L. 1974. Al/Si order and symmetry of natural alkali feldspars, and the relationship of strained cell parameters to bulk composition. Bull. Soc. Fr. Mineral. Crystallogr., 97, 336-377.

Winchester, J. A. & Floyd, P. A. 1977. Geochemical discrimination of different magma series and their differentiation products using immobile elements. Chem. Geol., 20, 325-343.

Tarmo Kiipli (a) and Toivo Kallaste (b)

(a) Mining Institute, Tallinn Technical University, Kopli 82, 10142 Tallinn, Estonia;tarmo.kiipli@egk.ee

(b) Institute of Geology, Tallinn Technical University, Estonia pst. 7, 10143 Tallinn, Estonia; kallaste@egk.ee
Table 1. Correlated volcanic beds (rows) from the studied core sections
(depth in metres)

Bed No. Bed No. Kiriku- Viire- Loetsa * Paha-
(Kiipli (Kiipli kula * laid * pilli *
 1998) et al.
 2001)

 25 29
 24 28
 23 27 20.85#
 new
 22 26 12.59#
 20 23 15.80 65.90# 44.40# 40.30#
 19 21
 18 22 17.20#
 17 19 17.85# 66.60# 45.10#
 18 67.75
 16 17 68.30 47.20# 45.20#
 14 16 46.20
 new
 12 15 28.25# 51.50
 new
 14 76.45#
 11 13 76.70# 56.80# 61.70#

 9 12 77.60# 57.70# 64.60
 8 11 78.11# 65.65#
 7 10 78.20#
 6 9 78.48# 67.00#
 5 7 79.13# 68.50#
 6 79.38#
 4 5
 new
 3 4
 2 3 72.20#
 1 2
 0 0 38.16# 85.00 66.00# 78.35#

Bed No. Bed No. Valjala * Must- Nassu- Viki *
(Kiipli (Kiipli jala maa *
 1998) et al.
 2001)

 25 29 113.80#
 24 28 115.02#
 23 27 119.80# 121.03#
 new 69.80# 131.10#
 22 26 82.08# 199.70# 145.75#
 20 23 200.70# 147.50#
 19 21 148.00#
 18 22 85.40# 148.80#
 17 19 85.79# 201.80# 149.40
 18 151.80
 16 17
 14 16 152.10#
 new
 12 15 94.00# 156.80#
 new
 14
 11 13 105.95# 219.40# 169.60#

 9 12 109.63# 171.95#
 8 11 153.40 173.10#
 7 10 111.95# 174.40#
 6 9 175.55#
 5 7
 6
 4 5 178.80#
 new 117.80#
 3 4 181.80#
 2 3 182.30#
 1 2 184.35#
 0 0 165.40 124.70 235.10# 185.10#

Bed No. Bed No. Tehu- Kauga- Ohe- Aizpute
(Kiipli (Kiipli mardi tuma scare
 1998) et al.
 2001)

 25 29 340.76#
 24 28 236.90# 342.08# 917.10#
 23 27 243.20# 345.83# 925.80#
 new 256.00# 351.72# 931.80#
 22 26 163.91# 258.90 359.31
 20 23 361.30#
 19 21 261.10# 361.70# 938.00#
 18 22 165.90# 362.23# 941.35#
 17 19 166.70# 261.50# 362.46#
 18 263.10 364.76 943.90#
 16 17 365.08 946.90#
 14 16 950.10#
 new 264.80# 367.39 951.20#
 12 15 170.30# 264.90 367.60# 951.70#
 new 369.12 953.99#
 14 369.72
 11 13 267.00# 369.75# 954.20#

 9 12
 8 11 184.03# 267.10#
 7 10 185.10# 369.98# 957.10#
 6 9 185.80# 267.20# 957.75#
 5 7 186.70# 370.09#
 6 187.65# 370.44#
 4 5 188.10# 370.63# 960.20#
 new 190.30#
 3 4 268.60#
 2 3 191.95#
 1 2 370.77# 963.80#
 0 0 193.70# 269.60# 964.40#

 Main component
Bed No. Bed No. of K-Na sanidine
(Kiipli (Kiipli
 1998) et al. NaAl[Si.sub.3] Width of the
 2001) Og, mol% reflection, deg

 Much of biotite and quartz,
 25 29 little sanidine
 24 28 35.2-35.8 0.19-0.34
 23 27 380 0.25-0.35
 new 36.2-37.8 0.08-0.12
 22 26 Very wide reflection
 20 23 45.2-46.3 0.12-0.20
 19 21 42.0-42.8 0.18-0.27
 18 22 Very wide reflection
 17 19 45.7-46.4 0.05-0.09
 18 Very wide reflection
 16 17 Very wide reflection
 14 16 Very wide reflection
 new 45.0-45.8 0.12-0.17
 12 15 Very wide reflection
 new 45.50 0.09
 14 22.60 0.05
 11 13 22.9-23.3 0.04-0.06
 Much of biotite and quartz,
 9 12 little sanidine
 8 11 38.7-40.3 0.10-0.16
 7 10 25.8-26.7 0.07-0.10
 6 9 25.5-26.2 0.25-0.30
 5 7 20.5-24.1 0.30-0.34
 6 28.1-28.8 0.07-0.08
 4 5 40.1-40.6 0.17-0.19
 new 24.5-25.3 0.05-0.11
 3 4 Very wide reflection
 2 3 45.2-47.6 0.12-0.17
 1 2 Very wide reflection
 0 0 20.7-21.5 0.05-0.09

Bold--volcanic beds where sanidine was studied; normal font--beds
correlated by trace elements; small font--supposed correlations.

* Cores where trace elements were studied in volcanic beds (Kiipli
1998; Kiipli & Tsegelnjuk 2001).

Note: Volcanic beds where sanidine was studied; normal font--beds
correlated by trace elements; small font--supposed correlations
indicated with #.

Table 2. List of volcanic beds not correlated with other sections

 Bed No. Bed No.
 (Kiipli (Kiipli Core
 1998) et al.
 2001)

 21 25 Kirikukula
 4 Viirelaid
 Mustjala
 Tehumardi
 Kaugatuma
 Ohesaare
 Aizpute
 -1 -1 Pahapilli

 Core Depth, Main component
 m of K -Na sanidine

 NaAl Width
 [Si.sub.3] of the
 [O.sub.8], reflection,
 mol% deg

Kirikukula 15.50 Very wide reflection
Viirelaid 79.44 26.2 0.26
Mustjala 115.87 47.3 0.12
Tehumardi 179.90 Very wide reflection
Kaugatuma 262.20 46.6 0.08
Ohesaare 370.99 35.3 0.19
Aizpute 956.30 Very wide reflection
Pahapilli 83.85 Very wide reflection

Fig. 1. Stratigraphic chart according to Nestor (1997) and Kaljo et al.
(1998).

INTERNATIONAL ESTONIA LATVIA
 REGIONAL FORMATIONS FORMATIONS
SERIES STAGES

Wenlock Jaagarahu Jaagarahu
 Jaani Jaani Riga

Llandovery Adavere Velise Jurmala
 Rumba Dobele
 Raikkula Raikkula
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Author:Kiipli, Tarmo; Kallaste, Toivo
Publication:Proceedings of the Estonian Academy of Sciences: Geology
Date:Sep 1, 2002
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