High-frequency cyclicity in a Miocene sequence of the Vienna Basin established from high-resolution logs and robust chronostratigraphic tuning

Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

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Palaeogeography, Palaeoclimatology, Palaeoecology j o u r n a l h o m e p a g e : w w w. e l s ev i e r. c o m / l o c a t e / p a l a e o

High-frequency cyclicity in a Miocene sequence of the Vienna Basin established from high-resolution logs and robust chronostratigraphic tuning Wieske E. Paulissen ⁎, Stefan M. Luthi Department of Geotechnology, Delft University of Technology, Stevinweg 1, 2628 CN Delft, The Netherlands

a r t i c l e

i n f o

Article history: Received 7 February 2011 Received in revised form 26 April 2011 Accepted 16 May 2011 Available online 24 May 2011 Keywords: Integrated stratigraphy Sedimentation rates Cyclostratigraphy Milankovitch cycles Sub-Milankovitch cycles Vienna Basin

a b s t r a c t A high-resolution chronostratigraphic record established by [W.E. Paulissen, S.M. Luthi, P. Grunert, S. Ćorić, M. Harzhauser, Geol. Carp. (2011)] that takes into account variations in sedimentation rates and temporal gaps caused by unconformities and faulting in a research borehole in the Vienna Basin was used to investigate the possible presence of orbital, millennial and centennial periodicities. The sedimentary sequence covers Middle to Late Miocene shallow marine, fluvio-deltaic and lacustrine shales, silt- and sandstones deposited during the transition from a pull-apart basin to the final infill in a compressional regime. Spectral analysis was performed on gamma ray logs and high-resolution electrical borehole images using three different analytical methods over six suitable intervals where continuous and constant sedimentation was identified. The significant periods were found to closely match the orbital cycles of precession, obliquity and short eccentricity, providing a solid basis for the analysis of potential sub-Milankovitch cycles. The significant frequencies encountered at the millennial- to centennial-scale fell for 75% within a relatively narrow time period of 0.25 to 5 kyr, with a concentration of peaks between 1 and 2 kyr (29%) and 500 to 800 years (17%). These periodicities relate closely to the millennial- (Dansgaard–Oeschger and Bond cycles) and centennial-scale climate cycles documented from the Quaternary. It is suggested that the high-frequency cycles observed in the Miocene of the Vienna Basin represent differences in grain size related to cyclic variations in regional precipitation. © 2011 Elsevier B.V. All rights reserved.

1. Introduction The study of cyclic patterns in sedimentary records has a long history, mostly because of the often conspicuous rhythmicities observed in many stratigraphic sequences (Einsele et al., 1991, p. 1–19). Detecting cyclic sedimentation patterns and assigning them in a hierarchical manner to different processes and temporal periodicities help the geoscientists understand the origin of sedimentary sequences and the importance of the various driving mechanisms. Thus, many researchers have suggested that orbital cycles influence sedimentary records, initially mostly based on deep sea sediments (Hays et al., 1976; Imbrie and Imbrie, 1979; Imbrie et al., 1984), which lent substantial support to the Milankovitch theory on climate change. Currently there are numerous publications every year documenting cyclicities in the sedimentary record, many of them still from depositional environments with relatively continuous sedimentation, for which a link between orbital climate forcing and sedimentation is suggested. Deposits from shallow water environments have also been studied (e.g. García et al., 1996; van Vugt et al., 2001; Napoleone et al., 2004; Sacchi and Müller, 2004; Steenbrink et al., 2006; Abels et al., 2009), but these are often characterised by substantial sedimentary gaps and sudden changes in

⁎ Corresponding author. E-mail address: [email protected] (W.E. Paulissen). 0031-0182/$ – see front matter © 2011 Elsevier B.V. All rights reserved. doi:10.1016/j.palaeo.2011.05.029

sedimentation rates. Age dating in these sequences often does not have the required resolution and accuracy in order to establish the potential imprint of orbital cyclic forcing on the sedimentary record. Therefore, an autocyclic origin often has to be considered as an alternative option to explain rhythmic patterns in such sequences (Burgess, 2006; Muto et al., 2007). Deposits from shallow water environments often also show rapid shifting of the facies belts, resulting in sequences that may not contain sufficient geological time for the longest orbital periodicities (long and short eccentricity) to be detected. These longer cycles are used by a number of authors to constrain the shorter Milankovitch periodicities, attributed to obliquity and precession, in rhythmic sedimentary sequences (e.g. Gale et al., 1999; Weedon et al., 1999; Preto et al., 2001; Lirer et al., 2009). Even shorter periodicities, the so-called millennial- and centennial-scale cycles, have been identified with this approach (Zühlke et al., 2003; Mawson and Tucker, 2009; Boulila et al., 2010). This paper is based on an approach in which sedimentation rates and hiatuses are determined to a high degree of accuracy with a combination of stratigraphic methods. The depositional setting is in the Miocene of the Paratethyan Vienna Basin and is known to contain stratigraphic gaps and highly variable sedimentation rates (Harzhauser and Piller, 2004; Kováč et al., 2004). This integrated approach combines biostratigraphy, magnetostratigraphy, seismic stratigraphy and lithostratigraphy in a borehole that could be used for research purposes (Paulissen et al., 2011). Age dating of the sediments is obtained from a continuous

W.E. Paulissen, S.M. Luthi / Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

The spectral analysis is applied on conventional wireline logs, such as the gamma ray log, as well as on electrical borehole images that have a much higher resolution of about 1 cm (the sampling rate is 0.25 cm). Logs have been previously used to analyse potential periodicities in sedimentary sequences (Barthès et al., 1999; Harzhauser and Piller, 2004; Harzhauser et al., 2004; Sacchi and Müller, 2004; Lefranc et al., 2008; Lirer et al., 2009), but the link between the physical characteristics recorded by wireline logs in boreholes and the depositional or diagenetic processes that causes them is often difficult to establish. The methodology described here thus does not use the a priori assumption that an orbital signal is preserved in the sedimentary record that can be used to establish a high-resolution time calibration (so-called orbital tuning). Rather, it seeks to determine first a high-

Spectral

Low High

Milankovitch

Intervals

Terrestrial/ Fluvial

6 C4Ar

Upper

9.5

Pannonian

9.0

C5n

Middle Lower

Pannonian

Tortonian

11.0

4

Pannonian

10.5

Upper Miocene

5 10.0

Vienna Basin Depositional environment

GR analysis

Millennial

1.50

Sedimentation rate (m/kyr)

0.50

Polarity

Chronozones

GPTS

C4An

Central Paratethys stages

Stage

Epoch

Time (Ma)

magnetostratigraphic record by a palaeomagnetic logging tool, combined with biostratigraphic analysis of borehole cuttings that provides the tie-in points to connect the magnetic polarities to the Geomagnetic Polarity Time Scale (GPTS). Seismic data is used to identify temporal gaps in the sedimentary record, caused either by erosion, nondeposition or faulting. The faults identified on the seismic data are then identified on electrical borehole images, resulting in exact locations of these stratigraphic gaps in the borehole. This chronostratigraphic framework is used to determine a complete record of sedimentation rates that takes into account the temporal gaps. It also allows the definition of intervals that are suitable for spectral analysis; these intervals should be devoid of hiatuses and contain relatively constant sedimentation rates.

1.00

314

m7

m6

Terrestrial

Lacustrine/ Proximal deltaic

3 2

Lacustrine/ Distal deltaic

m5 m4

C5An

Restricted marine/ Deltaic

m3 m2 m1

1

Restricted marine/ Deltaic

C5Ar

Upper

Sarmatian

Lower

Serravalian

Sarmatian

12.5

Middle Miocene

12.0

C5r

11.5

Fig. 1. Chronostratigraphic framework of the research well according to Paulissen et al. (2011) based on seismic data, well correlation, biostratigraphy and magnetostratigraphy for the Sarmatian and Pannonian interval. The Central Paratethyan stages are according to Harzhauser and Piller 2004, Harzhauser et al. (2004) and Strauss et al. (2006) and the Geomagnetic Polarity Time Scale (GPTS) according to Lourens et al. (2004) with solid and dashed arrows on the GPTS indicating the short polarity subchrons and polarity fluctuations as described by Krijgsman and Kent (2004). The sedimentation rates are calculated for the magnetostratigraphic intervals through a combined stratigraphic approach and are not corrected for compaction. The gamma ray log (GR) was stretched linearly between the magnetostratigraphic tie-ins with the stratigraphic gaps taken into account.

W.E. Paulissen, S.M. Luthi / Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

resolution chronostratigraphic record that forms the basis for a subsequent analysis of periodicities. The following questions will be addressed in this paper: Can orbital forcing be demonstrated in the sedimentary cycles of the downhole sedimentary sequence available in this study? If orbital forcing is suggested, can higher-resolution periodicity at the millennial- or centennial-scale (sub-Milankovitch scale) be distinguished? What are the relative contributions of allocyclic, autocyclic and tectonic controls to the basin infill? 2. Chronostratigraphic framework A previous study of Paulissen et al. (2011) on the sedimentary sequence encountered in a borehole in the central part of the Paratethyan Vienna basin resulted in a reliable chronostratigraphic framework necessary for the spectral analysis presented here (Fig. 1). The borehole in which the analysis is carried out is approximately 2 km deep and covers the Middle to Late Miocene (Paulissen et al., 2011). The abundance of magnetic polarity reversals during this geologic time period (Lourens et al., 2004; Hüsing et al., 2007) makes it well suited for a high-resolution magnetostratigraphic study. Besides this a good micropalaeontological reference base exists for the Miocene in the Central Paratethys to provide an independent chronological constraint (Papp et al., 1978; Cicha et al., 1998). The Badenian, Sarmatian and Pannonian regional stages have been successfully identified, the latter two with great accuracy. The sedimentary sequence comprises a succession of shales, silty shales, siltstones and sandstones in a general coarsening-upward sequence (Fig. 1). The Badenian sediments consist of proximal deltaic facies alternating with shale-prone intervals deposited in a deeper marine environment (Kreutzer and Hlavatý, 1990; Kováč et al., 2004). During the Sarmatian deposition was predominantly deltaic in a restricted marine setting whereas from the Pannonian onwards most of the

315

Central Parathethyan became lacustrine (Harzhauser and Piller, 2004; Harzhauser et al., 2004; Kováč et al., 2004; Kováč et al., 2008), exhibiting a progradational pattern from distal to proximal deltaic and fluvial in the uppermost part. The entire sequence reflects the creation of accommodation space, peaking during the Sarmatian, and subsequent infilling of the Vienna Basin with detritus derived from the Bohemian massif and the newly formed Alps, ending with a bypass phase in the Upper Pannonian (Paulissen et al., 2011). Biostratigraphic analysis focused on the benthic foraminiferal content on the borehole cuttings and allowed the recognition of the Badenian as well as the Lower and Upper Sarmatian stages (Paulissen et al., 2011). The magnetostratigraphy in the Badenian, however, proved to be inconclusive and this stage is left out in the following. Stratigraphic gaps were identified at the bottom of the lower Sarmatian substage, between the lower and upper Sarmatian and at the top of the upper Sarmatian through a combination of magnetostratigraphy, seismic sequence stratigraphy and well correlation with two adjacent wells. The Pannonian interval showed a more continuous stratigraphic record with only one major stratigraphic gap in the upper Pannonian, but with significant variations in sedimentation rates as evidenced primarily from magnetostratigraphy. The sedimentation rates after compaction ranged from around 0.5 to over 1.2 m/kyr in the Sarmatian, and generally between 0.25 and 0.5 m/kyr in the Pannonian (Fig. 1). They are not corrected for the slight borehole deviation and the low tectonic dip. 3. Methods 3.1. Conventional and high-resolution log data The wireline logs used for the spectral analysis are the gamma ray log and the electrical borehole images, recorded in two separate

FMI image Orientation North 0

Depth (m) 627

Resistive

120

240 FMI Image

Background Conductivity 360 300 Conductive

( mS/m )

1100

Gamma ray 75 ( gAPI ) 150

Conductivity −500

( mS/m)

2000

628

629

630

631

632

633 Fig. 2. Detailed logs between 633 and 627 m from interval 2 (670–550 m) highlighting the differences in resolution between the logs. The Fullbore Formation MicroImager (FMI) image shows well defined layering with bright beds being more resistive and dark beds more conductive. The background conductivity curve is a result of the BorTex program and only displays the borehole crossing features while the curve labelled Conductivity is the response of one single electrode button from the FMI.

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Table 1 List of the selected intervals for spectral analysis to check for Milankovitch cycles (see Fig. 1 for locations). The sedimentation rates were determined through a combined stratigraphic approach (Paulissen et al., 2011) and were used to calculate the presumed length of the 100 kyr eccentricity, 41 kyr obliquity and 23 and 19 kyr precession cycles in metres for comparison with the spectral results. Interval

Depth (MD)

Interval thickness (m)

Sed. rate (m/kyr)

1

1269–1168 1168–1125 670–634.5 634.5–550 513–478 422–367.5 287–249 249–231.5 171.5–139 139–84

144

0.49 0.47 0.46 0.47 0.27 0.24 0.24 0.28 0.33 0.26

2 3 4 5 6

120 35 45.5 45.5 87.5

Orbital periods (kyr) 100

41

23

19

49 47 46 47 27 24 24 28 33 26

20.1 19.3 18.9 19.3 11.1 9.8 9.8 11.5 13.5 10.7

11.3 10.8 10.6 10.8 6.2 5.5 5.5 6.4 7.6 6.0

9.3 8.9 8.7 8.9 5.1 4.6 4.6 5.3 6.3 4.9

runs (intervals) in the borehole and covering the entire well. The electrical borehole images were acquired with the Fullbore Formation MicroImager (FMI, Mark of Schumberger) and provide a resistivity image of the borehole wall from microresistivity measurements of 192 electrodes with a vertical and azimuthal sampling rate of 0.25 cm (Luthi, 2001). From these images, sedimentary and tectonic structures such as bedding planes, faults and fractures can be identified with a resolution of about 1 cm. For a sedimentation rate of 0.25 m/kyr the resolution of the gamma ray of about 60 cm corresponds to a resolution of 2400 years in geologic time, whereas the higher resolution of the FMI of 1 cm represents 40 years, and twice as much for both cases if the sedimentation rate is doubled. Thus the electrical borehole images potentially allow the detection of millennial- to centennial-scale periodicities if the sedimentation rates are high enough. Theoretically, a sedimentation rate of as low as 0.01 m/kyr allows the detection of a 1000-year cycle, but higher sedimentation rates obviously increase the significance as more samples will be contained in 1 cycle. 3.2. Log processing The electrical borehole images from the FMI were processed and quality-checked following the procedure described by Luthi (2001). Fig. 2 shows the FMI images oriented with respect to North, with the grey-scale indicating the conductivity levels: white for low and black for high conductivities. Two one-dimensional curves were used for the spectral analysis. The first curve is simply one of the 192 channels of the electrical borehole image. However by just using one channel there is the risk of missing geological information due to local borehole disturbances, noise or heterogeneities such as bioturbation that affect layering. A second curve was therefore computed with the goal to retain primarily the layering information and to exclude heterogeneities and local borehole artefacts. The BorTex software (Mark of Schlumberger) was used to extract those features that show lateral continuity along the layer dip and across the entire borehole (Delhomme, 1992; Al-Rougha, 2005; Lefranc et al., 2008). The resulting log is thus a background conductivity log representing essentially layering characteristics. A short borehole interval of the three logs used for the spectral analyses is shown in Fig. 2. The gamma ray exhibits a very

indistinct, sluggish response that is, however, well suitable for the analysis of longer cyclicities. The background conductivity log is seen to be a low-pass filtered curve of the FMI image, whereas the single-channel conductivity log exhibits more details including fine-scale layering, but with the risk of containing data unrelated to layering. The background conductivity and the single-channel conductivity curves can be compared for consistency in their spectral content when using them for the analysis of millennial- to centennial-scale cyclicity.

3.3. Selection of study intervals The intervals selected for spectral analysis for the Milankovitch and millennial- to centennial-scale cycles are indicated in Fig. 1. To capture orbital forcing influences the selected intervals had to be large enough to capture several cycle lengths of the potential Milankovitch cycles, to have good chronostratigraphic calibration points and relatively constant sedimentation rates (Table 1). Additionally, each interval contains sediments that were deposited in the same sedimentary environment and consist of the same general lithology (Fig. 1). In Table 1 the depths of these selected intervals are displayed with the interval thicknesses and their sedimentation rates. From the sedimentation rates the presumed lengths of the Milankovitch cycles for short eccentricity, obliquity and precession were calculated for comparison with the spectral results. For the millennial- to centennial-scale cyclicities the electrical borehole images were used to search for apparent cyclicity in the intervals where fine-scale layering was present as in Fig. 2.

3.4. Spectral analyses In order to understand the major properties of the signals and to avoid mathematical artefacts that can be caused by one specific method a combination of different spectral analysis techniques has been applied on the data sets. These include two spectral estimators based on classical Fourier analysis, the Blackman–Tukey (BT) windowed correlogram (Blackman and Tuckey, 1958) using the SSA-MTM Toolkit of Ghil et al. (2002) and the Monte Carlo CLEAN procedure (Heslop and Dekkers, 2002) that is able to determine the frequency distribution of unevenly spaced (Roberts et al., 1987) and noisy data series (Baisch and Bokelmann, 1999). The Monte Carlobased method described by Heslop and Dekkers (2002) uses the CLEAN algorithm of Roberts et al. (1987) to test for the significance levels in the resulting spectra. The method includes a series of Monte Carlo simulations with the addition of white noise, red noise or through a data-stripping method that each time generates a slightly different spectrum from which a mean spectrum and its confidence limits are determined. Prior to processing the mean values were subtracted from the data series and detrending was performed. For the Monte Carlo CLEAN procedure data stripping was applied to up to 50% of the original signal, and random stripping was performed 500 times. Then 100 simulations were performed which results in a significance level equivalent to 1000 separate simulations. Additionally the wavelet transform was applied using the code provided by Torrence and Compo (1998). The mother wavelet was set to the Morlet wavelet (ω0 = 6) where the wavelet scale can be regarded as equal to the Fourier period.

Fig. 3. Results for interval 2 (670–550 m) for three logs and three spectral analysis methods. Monte Carlo CLEAN was applied with the bootstrapping method. BT spectral analysis was carried out with a Bartlett smoothing window using a window size of 50% of the interval size. The 95% confidence interval in the wavelet power spectrum is enclosed with the grey line for a red-noise process with a lag-1 coefficient of 0.72 and the shaded contours are at normalised variances of 0.0625, 0.125, 0.25, 0.5, 1, 2, 4, 8, 16 and 32. Note the cone shaped thick line, outside this line edge effects become important. The global power spectrum displays the average spectrum of the wavelet power spectrum over the whole depth interval, the dashed line shows the 95% confidence interval. For further details see text.

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conductivity log used for the spectral analysis of the 120 m thick interval on Fig. 2 contains 47,244 data points. The log was therefore resampled to a 5 cm spacing by applying a sinc function interpolation

Because of the high sampling rate of the electrical borehole images the data size of the intervals for the spectral analysis was too large to perform the calculation. For example the background

Interval 2 ( 670-550 m) Gamma ray

Background conductivity

Power

24

2

1.2

16

97.5%

12

95%

0.8

8

0.4

4

16 99%

99% 12

97.5% 95%

97.5% 95%

4

102

101 Period (m)

Power

100

102 8

3

101 Period (m)

x105

100

102

101

100 Period (m)

x105 12

7

10

6 8

5

2

6

4 3

4

1 2

2

1 101 Period (m)

16

Period (m) 4 8

2

1

0.5

16

Period (m) 4 8 2

0

101

100 Period (m)

1

64

0.5 0.25

32

16

Period (m) 4 2 8

1

0.5 0.25

580 600

580

620 640 660

640

3

x105

x105 10

6

2

4

1

5

2 95%

0

102

620

620 640 660 x105 Power

32

10

600

600

Wavelet

64

101 Period (m)

560

560

32

102

580

Depth (m)

64

100

560

102

Global Spectrum

20

8

x103

Blackman Tukey

99%

1.6

660

Monte Carlo CLEAN

20

Conductivity

64

32

16

8 4 2 Period (m)

95%

95%

1

0.5

0

64

32

16

8 4 2 Period (m)

1

0.5 0.25

0

64

32

16

8 4 2 Period (m)

1

0.5 0.25

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W.E. Paulissen, S.M. Luthi / Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

and a zero-phase anti-alias filter (low-pass Gaussian). When analysing the smaller intervals for millennial- and centennial-scale cyclicities the borehole image data was however used in the original format. Fig. 3 displays the results for interval 2 (670–550 m) for the three logs and the three spectral analysis methods. The gamma ray and the conductivity logs produce the same spectral results for the Monte Carlo CLEAN procedure and the Blackman–Tukey method, with both having significant peaks at 8, 11 and 17 m. The local wavelet power spectrum also has significant peaks in the 95% confidence level for the same periods. The difference in resolution between the gamma ray and the conductivity logs is evident from the presence of additional significant peaks in the 0.5–10 m range for the conductivity logs. The spectral contents of the background and single-channel conductivity log are found to be very similar and therefore the background conductivity log is used for the spectral analysis on the Milankovitch scale. Since the Monte Carlo CLEAN procedure quantifies the significance levels its results will be used in the further discussion of the spectral results for all intervals.

4. Orbital forcing The spectra obtained with the Monte Carlo CLEAN procedure for the six selected depth intervals are shown in Fig. 4 with the 95%, 97.5% and 99% confidence levels and the sedimentation rates used to convert the peak values from depth to time (in kyr). Some intervals include two similar sedimentation rates and in those cases both are indicated and two periodicities are calculated. For peaks on the power spectra that are judged significant and that correspond to or approximate a Milankovitch orbital cycle the periods are indicated in kyr (rounded to integers). The Milankovitch cycles considered here are the short eccentricity of 100 kyr, obliquity of 41 kyr and precessions of 23 and 19 kyr. The number of Milankovitch cycles that can be expected in each interval are calculated in Table 2. Intervals 1, 2 and 6 are seen to be long enough to contain approximately three short eccentricity cycles, and this period is indeed seen in intervals 2 and 6 in Fig. 4. Furthermore all intervals reveal peaks above the 95% confidence level and sometimes above 99% that closely match the 41 kyr obliquity cycle as well as the 19 and 23 kyr precession cycle. Only the peak in interval 3 with a period of 11 m with a calculated duration of 41 kyr is slightly below the 95% confidence line and was therefore not included as a significant period in Fig. 4. Relatively few peaks in the Milankovitch scale do not fall within about a 10% range of the four orbital periods. To further evaluate the possible presence of the longer Milankovitch periods the background conductivity curve covering the middle to upper Pannonian interval was converted to time (9.58–10.52 Ma) using the chronostratigraphic framework from Fig. 1. The log was interpolated linearly between the magnetostratigraphic tie-in points and resampled to obtain an even sampling of 0.2 kyr (Fig. 5). Besides the periods for obliquity and precession the spectra now also reveal two distinct peaks at 129–133 kyr and 93 kyr that closely approximate the periods for long (125 kyr) and short (95 kyr) eccentricity (Fig. 5). The spectrum shows a good fit with the eccentricity target curve of Laskar et al. (2004) shown on top in Fig. 5. Additionally all spectra show significant peaks in the subMilankovitch range. Intervals 1 to 3, covering the Sarmatian and the lower Pannonian, show significant peaks, or almost significant in the case of interval 3 (93%), at the millennial-scale around 1.8, 1.4 and 1.5 kyr. For the upper three intervals 4 to 6, covering the middle to upper Pannonian, the shortest significant peaks lie between 5 and 7 kyr and are thus longer than in the lower three intervals. The electrical borehole images in the lower intervals exhibit clear cyclic layering and were therefore further analysed in more detail.

5. Millennial- to centennial-scale cyclicity Seven intervals were selected for a detailed analysis of subMilankovitch cycles. They were chosen based on the orbital frequency analysis results discussed above and the degree of rhythmic bedding such as the example shown in Fig. 2. They all consist of shale- and siltprone lithologies, with some lying within the previously analysed intervals, but others outside. Fig. 1 shows their locations and Table 3 summarizes their characteristics. Due to the difference in length and in sedimentation rates the intervals range between 9 and 89 kyr in duration (Table 3). Comparison of the spectra obtained from the background conductivity curve and from a single-channel conductivity curve from the FMI image for interval m4 shows that on the millennial-scale the two curves produce similar results for the most significant peaks (Fig. 6). The most prominent period in both spectra has a duration of 1.77 kyr followed by others at 3.8, 1.46 and 0.77 kyr. Due to the higher variability and frequency content of the conductivity curve the overall power of its spectrum is higher and more significant peaks emerge at the centennial scale. For all intervals, therefore, the subsequent analysis was performed using single-channel conductivity curves. All resulting peaks above the 99% significance threshold in the power spectra were selected and converted to periods (in kyr) using the interval sedimentation rates. The resulting periods were sorted in a histogram by grouping the number of peaks within a bin size of δt = log(0.1) (Fig. 7). The histogram shows a distribution with 75% of all significant peaks falling within the range between 0.25 and 5 kyr, 29% in the interval between 1 and 2 kyr, and 17% between 500 and 800 years (Fig. 7). Two intervals in the lower Pannonian (m4 and m6) were long enough in duration to capture the signal of a possible precession cycle of 17 kyr for m4 and 23.7 as well as a 18.8 kyr peak for m6. 6. Discussion 6.1. Orbital forcing We analysed the possibility of orbital forcing and millennial- to centennial-scale cyclicities with a previously established robust chronostratigraphic framework. The investigated intervals from the Middle to Late Miocene sedimentary sequence showed constant sedimentation rates and were long enough to comprise several orbital cycles of obliquity and where possible of short eccentricity. The six selected intervals differ in sedimentation rates, stratigraphic ages and depositional environments. In all cases the spectral results revealed significant periods with durations that closely match the orbital cycles of precession, obliquity and short eccentricity. Obliquity appears to be the strongest signal except for intervals 2 and 3 in the lower Pannonian, with precession being more pronounced in the first and eccentricity in the latter. Analysis of a longer time interval in the Pannonian also indicates two components that are interpreted as the result of orbitally controlled short eccentricity cycles. It thus seems that astronomical forcing seems to have played a significant role, at least during the time intervals studied here, in the sedimentation processes that drove the infill of the Vienna Basin during the Middle to Late Miocene. Previous studies have reported sedimentary cyclicities in the Miocene from deep marine and continental sections in the Mediterranean region, interpreted to be caused by orbitally induced variations in insolation (Hilgen, 1991a,b; Abdul Aziz et al., 2003; Hilgen et al., 2003; Lourens et al., 2004; Hüsing et al., 2007; Abdul Aziz et al., 2008; Abels et al., 2009). Other studies on the Miocene were conducted on climate proxy records from DSDP and ODP sites (e.g. Shackleton and Crowhurst, 1997; Holbourn et al., 2007; Abdul Aziz et al., 2008). Two continuous ODP sedimentary records in the northwestern and southeastern Pacific with δ 18O and δ 14C isotopes were astronomically

W.E. Paulissen, S.M. Luthi / Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

20 51 49

60

0.49 m/kyr 0.47 m/kyr

1

18

102 105

0.46 m/kyr 0.47 m/kyr

16

50

30 20

37 36

18 17

99%

25 23 22 21

Power

Power

40

19 19

12 10

25 25

8

97.5%

2

37 38

14 82 78

319

6

95%

4

10

2 102

101

100

102

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100

Period (m)

Period (m) 25 0.27 m/kyr

3

20

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0.24 m/kyr

100

4

41

Power

Power

90

15 18 21

80 23

60

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10 40 5

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70

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0.33 m/kyr 0.26 m/kyr

60 41

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38

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Power

80 60 42

18 16 21

40

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43

104 23 17 18

40 30 20

20 102

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100

Period (m)

102

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100

Period (m)

Fig. 4. Spectral analysis results obtained with the Monte Carlo CLEAN procedure for the six selected intervals to analyse potential orbital forcing. The confidence levels are displayed for 95%, 97.5% and 99% and the displayed sedimentation rates (Table 1) were used to convert the peak values from depth to time (kyr). Only the peaks that are judged significant (above 95%) and that correspond to or approximate the Milankovitch cycles of short eccentricity, obliquity and precession are indicated by numbers in kyr.

tuned by Holbourn et al. (2007) on the climate transition interval of 17.1–12.7 Ma. They mentioned an ‘Icehouse mode’ after 13.9 Ma with distinct 100 kyr variability and significant power in the 41 kyr band suggesting that eccentricity was a prime pacemaker of middle Miocene climate evolution, and that obliquity-paced changes in high-latitude seasonality favoured the transition into the ‘Icehouse’ climate. For the Upper Miocene (10.3–9.2 Ma) Abels et al. (2009) reports mainly precession-driven lithofacies cycles in continental deposits in the Teruel Basin (Northeast Spain), with obliquity influences only occurring during 405 kyr eccentricity minima. For the Paratethyan region there are only few cyclostratigraphic studies on Miocene deposits. In the Vienna Basin Harzhauser and Piller (2004), Harzhauser et al. (2004), Hohenegger et al. (2009), and Lirer et al. (2009) have performed orbital tuning on sedimentary

records using well logs, but due to limited chronostratigraphic control the results need to be considered with caution. Lirer et al. (2009) concludes that a 41 kyr period is missing in the lower Pannonian, whereas our study suggests that it is significant and other authors report it to be omnipresent for the coeval early Tortonian–Serravallian time interval in the Mediterranean region (Hilgen et al., 2000; Turco et al., 2001; Hilgen et al., 2003; Hüsing et al., 2007). This loss of obliquity control led Lirer et al. (2009) to the conclusion that the communication between the Central Paratethyan and Mediterranean realms must have ceased from the Lower Pannonian onwards. The well on which their research was based is in the vicinity of our research well (approximately 15 km NNE) so the sedimentary conditions must have been similar. Their results are however contradicting with our evidence that obliquity-controlled cyclicity is

W.E. Paulissen, S.M. Luthi / Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

Table 2 Number of orbital periods expected for each interval calculated by dividing the interval thickness by the presumed length of the orbital period.

100

41

23

19

1

2.9 3.1 2.6 2.6 1.3 1.9 1.9 1.6 2.7 3.4

7.2 7.5 6.4 6.2 3.2 4.6 4.6 4.0 6.5 8.2

12.8 13.3 11.3 11.1 5.6 8.2 8.2 7.1 11.5 14.6

15.5 16.1 13.7 13.4 6.8 10.0 10.0 8.6 14.0 17.7

6

Eccentricity (Laskar 2004)

467-415 95

78 54

178

101

102

Period (kyr) 140 311 467

BC 9.58−10.52 Ma 133-129 113 93

100

60 187

64 81 37 40 51

99%

23 20

97.5% 95%

20 102

101

100

Period (kyr) Background Conductivity (mS/m)

Period (kyr)

2

1

2

4

8

16

32

Time (Ma)

64

Although the intervals selected for analysis of the millennial- to centennial-scale cyclicity cover a range of stratigraphic ages and sedimentation rates, the frequency histogram (Fig. 7) indicates that most significant frequencies fall within a relatively narrow time frame of 0.25–5 kyr, with two distinct concentrations of peaks located between 500 and 800 years and 1–2 kyr. Millennial-scale cycles are well documented in stratigraphic records from the late Neogene and Quaternary deposits from polar to tropical latitudes from both hemispheres and from different sedimentary environments (Versteegh, 2005, and references therein). The main periods reported are clustered around 1.5 kyr and 2.5 kyr (e.g. Bond et al., 1997; van Geel et al., 1999). The best documented millennial cycles in the Pleistocene are referred to as Dansgaard– Oeschger events (Dansgaard et al., 1993), and those from the Holocene as Bond events (Bond et al., 1997, 2001). Both have a period of around 1470 years and are attributed to climate changes. Pre-Neogene records of millennial climate scale variability are scarce primarily due to limitations in chronologic constraining. Evidence for millennial-scale cycles in the Mesozoic is reported by Kent et al. (2004) and in the Palaeozoic by Anderson (1982), Elrick and Hinnov (2007), Mawson and Tucker (2009) and Tucker et al. (2009). The driving mechanisms leading to millennial-scale cycles are still unclear. Possibilities include internal feedback mechanisms within the ocean–atmosphere system or externally forced through variations in solar activity (van Geel et al., 1999; Bond et al., 2001) or long period ocean-tides (Keeling and Whorf, 2000; Munk et al., 2002). Because of the seemingly ubiquitous nature of these cycles through geologic time and space Elrick and Hinnov (2007) posit that it may be difficult to explain these cycles through internally driven thermohaline oceanic

2

128

6.2. Millennial- to centennial-scale cyclicity

4

256

present during the Pannonian. This difference could be explained by the fact that they assumed one constant sedimentation rate for the entire Sarmatian and Pannonian interval and thus a mismatch with the Milankovitch periodicities. In the adjacent Pannonian Basin several authors also attempted to connect Upper Miocene high-frequency sedimentary cycles to precession and short and long eccentricity cycles (Sprovieri et al., 2003; Sacchi and Müller, 2004), and precession, obliquity and long eccentricity (Juhász et al., 1997; Juhász et al., 1999). Sprovieri et al. (2003) proposed a mutual interaction of the climate subsystems that developed over the Mediterranean area and the central-eastern Europe continent and that these were orbitally forced. Our results based on carefully tuned chronostratigraphic control indicate that Milankovitch cycle signals are strong in our stratigraphic record, albeit with variable intensities in the different stratigraphic intervals. This is considered to form a solid basis for the analysis of sub-Milankovitch cycles.

Power

Orbital periods (kyr)

3 4 5

6

125

Interval

2

x 10-3

Power

320

4 x103

9.6

9.7

9.8

9.9

10.0

10.1

10.2

10.3

10.4

10.5 e1 e2

O P1P2

41 kyr

100 kyr

Fig. 5. Spectral analysis on the middle to upper Pannonian background conductivity (BC) time-series (9.58–10.52 Ma) using wavelet analysis and the Monte Carlo CLEAN procedure with all ages on the peaks displayed in kyr. The time-series was interpolated to constant intervals of 0.2 kyr prior to spectral analysis and is plotted with the 100 kyr (dark grey line) and 41 kyr (light grey line) filtered components. The two short eccentricities (e1 and e2), the obliquity (O) and precession cycles (P1 and P2) are indicated with a dashed line on the wavelet power spectrum. The power spectrum of the eccentricity target curve of Laskar et al. (2004) (9.58–10.52 Ma) is plotted on top for comparison. Note that the ages indicated in grey are combination tones which are a result of the intermodulation of the fundamental frequencies of the short and long eccentricity cycles.

W.E. Paulissen, S.M. Luthi / Palaeogeography, Palaeoclimatology, Palaeoecology 307 (2011) 313–323

12

Table 3 List of the selected intervals used for spectral analysis to check for millennial- to centennial-scale cyclicity (see Fig. 1 for locations). Depth (MD)

Interval thickness (m)

Sed. rate (m/kyr)

Length (kyr)

Lithology

m1 m2 m3 m4 m5 m6 m7

1187–1180 1150–1136 1122–1111 784–760 680–675 653–612 495–485

7 14 11 24 5 41 10

0.49 0.47 1.26 0.39 0.56 0.46 0.27

14 30 9 62 9 89 37

Shale Shale Shale and silt Silty shale Siltstone Siltstone Siltstone

500-800 yrs 1-2 kyr 10

Percentage %

Interval

321

8

6

4

precession 2

oscillations or continental ice sheet instabilities. Rather, they suggest an external forcing mechanism such as solar forcing as the main driving process. Recent modelling by Braun et al. (2005) suggests that a 1470 year cycle may be caused by the superposition of the 87 year Gleissberg and the ∼210 year DeVries–Suess solar cycles. The periodicities we found in the sedimentary record from the Vienna Basin lie within the same time range as those in the studies mentioned above: The peaks within the 1–2 kyr range clearly overlap with the Dansgaard–Oeschger and Bond cycles. The 500–800 year periods have been encountered in a δ18O proxy speleothem record for the southern African climate from the Late Holocene (Tyson et al., 2002) and in a foraminiferal δ18O record from a Central-Mediterranean sediment core covering the last two millennia (Taricco et al., 2009). Furthermore Bond et al. (2001) reported centennial-scale cycles during the Holocene in the 300–500 year and 900–1100 year bands in proxies

BC

mS/m

mS/m

-2

-1.5

-1

0

0.5

1

1.5

2

Fig. 7. Frequency histogram in the time domain expressed as a percentage of the total peaks above 99% significance for the millennial- to centennial-scale intervals (m1–m7), determined from the single conductivity curve from the Fullbore Formation MicroImager (FMI) image. The horizontal scale has a bin size of δt = log(0.1).

of deep-sea sediment cores and Roth and Reijmer (2005) found ~380 year and 500–600 year quasi-periodic signals in Holocene slope sediments of the Great Bahama bank of climatic origin.

Interval m4 (784-760 m) 40

760

Cond 1.77

Power

30

765

-0.5

Period (log(kyr))

1500

1000

500

2000

1500

1000

500

0

Depth(m)

Cond

0

3.8 6.6 2.4

0.73 1.46

99.9%

0.5

20

99% 97.5% 95%

10

770

102

101

100

10-1

10-2

Period (m)

40

BC

775 3.8

780

Power

30

1.77 1.46

6.6

20

2.4

99.9%

0.73

99% 97.5%

10

95%

785

102

101

100

10-1

10-2

Period (m)

Fig. 6. Comparison of the spectral results from a single-channel conductivity curve (Cond) and the background conductivity curve (BC) from interval m4 (784–760 m). The displayed peaks are in kyr and have been converted from the depth to time domain using the corresponding sedimentation rate of 0.39 m/kyr (Table 3).

322

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It lies outside the scope of this paper though to relate the observed millennial and centennial periodicities to a driving mechanism. The data used in our study are physical measurements using wireline logs in a borehole, and it is at this point not clear what exactly causes the small-scale variations in electrical conductivity of the traversed sequence. Mineralogical analyses on cuttings from interval m6 (Fig. 1 and Table 3) show two recurring main lithologies, both immature siltstones, one with abundant hematite coating, the other without coating but with abundant coal fragments. These differences might account for the changes in resistivities and could be caused by cyclic variations in the regional precipitation and weathering pattern. 6.3. Autogenic versus allogenic forcing In the lower Pannonian a set of deltaic progradation packages can be seen on the gamma ray log in Fig. 1. The progradation and retrogradation recurrences of these deltaic bodies in the lower Pannonian range in duration from 150 to 280 kyr and cannot be attributed to orbital forcing. Rather, they are likely to represent autogenic processes such as delta lobe switching (Stouthamer and Berendsen, 2007; Kim and Jerolmack, 2008). Within these deltaic progradation packages, however, higher-frequency cycles are discernible (in interval 2, see Fig. 1 and Fig. 4) that are here interpreted to be related to precession and obliquity cycles. This stratigraphic sequence therefore is the result of the superposition of allogenic and autogenic processes (Muto et al., 2007; Martin et al., 2009). On a larger scale, the infill history of the Vienna Basin can equally be seen as the results of two superposed processes, i.e. regional tectonism that is modulated by orbital influences. The millennial- to centennial cycles documented here add a third component to the controls of sedimentation in this basin, but to establish its driving mechanism needs considerable additional research. Acknowledgements This research is supported by the Netherlands Research Centre for Integrated Solid Earth Science (ISES). We are grateful to OMV for providing access to the well and for permission to publish the results. We would like to thank Fabrizio Lirer and an anonymous referee for their valuable comments on the manuscript. OMV and Schlumberger Wireline Services are thanked for financial support. Finally we thank Fuqiang Lai for technical assistance and Schlumberger for providing the Geoframe software and support in processing the data. References Abdul Aziz, H.A., Di Stefano, A., Foresi, L.M., Hilgen, F.J., Laccarino, S.M., Kuiper, K.F., Lirer, F., Salvatorini, G., Turco, E., 2008. Integrated stratigraphy and Ar-40/Ar-39 chronology of early Middle Miocene sediments from DSDP Leg 42A, Site 372 (Western Mediterranean). Palaeogeography, Palaeoclimatology, Palaeoecology 257 (1–2), 123–138. Abdul Aziz, H.A., Krijgsman, W., Hilgen, F.J., Wilson, D.S., Calvo, J.P., 2003. An astronomical polarity timescale for the late middle Miocene based on cyclic continental sequences. Journal of Geophysical Research-Solid Earth 108 (B3). Abels, H.A., Abdul Aziz, H.A., Ventra, D., Hilgen, F.J., 2009. Orbital climate forcing in mudflat to marginal lacustrine deposits in the Miocene Teruel Basin (northeast Spain). Journal of Sedimentary Research 79 (11–12), 831–847. Al-Rougha, H.B., 2005. Heterogeneity quantification, fine-scale layering derived from image logs and cores. World oil 226 (10), 53–58. Anderson, R.Y., 1982. A long geoclimatic record from the Permian. Journal of Geophysical Research 87 (C9), 7285–7294. Baisch, S., Bokelmann, G.H.R., 1999. Spectral analysis with incomplete time series: an example from seismology. Computers and Geosciences 25 (7), 739–750. Barthès, V., Pozzi, J.P., Vibert-Charbonnel, P., Thibal, J., Meliérès, M.A., 1999. Highresolution chronostratigraphy from downhole susceptibility logging tuned by palaeoclimatic orbital frequencies. Earth and Planetary Science Letters 165 (1), 97–116. Blackman, R.B., Tuckey, J.W., 1958. The Measurement of Power Spectra from the Point of View of Communication Engineering. Dover publications, New York. Bond, G., Kromer, B., Beer, J., Muscheler, R., Evans, M.N., Showers, W., Hoffmann, S., Lotti-Bond, R., Hajdas, I., Bonani, G., 2001. Persistent solar influence on north Atlantic climate during the Holocene. Science 294 (5549), 2130–2136.

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