Definitive orbital control on the origin and preservation of Lofer cyclicity in the Late Triassic Dachstein platform

Definitive orbital control on the origin and preservation of Lofer cyclicity in the Late Triassic Dachstein platform | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article Definitive orbital control on the origin and preservation of Lofer cyclicity in the Late Triassic Dachstein platform Zsolt Vallner, János Haas, József Pálfy This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-4281587/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 26 Oct, 2025 Read the published version in Palaeogeography, Palaeoclimatology, Palaeoecology → Version 1 posted You are reading this latest preprint version Abstract The Upper Triassic Dachstein Limestone is an archetypal example of platform carbonate formation that consists of peritidal-subtidal Lofer cycles. However, despite a long history of study, their allocyclic vs autocyclic origin remains controversial. Using modern cyclostratigraphic methodology, here we revisit the archive data of the Dachstein Limestone in core Po-89 from the Transdanubian Range, Hungary. Analysis of high-resolution time series of the Lofer facies types, colour, greyscale, and lithology revealed several spectral peaks that are identified with the Milankovitch cycles. The Lofer cycles correspond to a robust peak with a period of 3.6 m that is the expression of precession cycles with a period 21.65 kyr. The sedimentary rate is 16.5 cm/kyr, thus the studied core section represents 2.5 Myr. Our model of cyclic carbonate deposition suggests that aquifer- and limno-eustasy were the most likely drivers of cyclic sea level changes. Differences in the depositional processes and preservation of the Lofer cycles led to variations in their completeness that is also orbitally controlled and responds primarily to long eccentricity forcing. We detected several sub-Milankovitch cycles, of which the 13.5, 7, 5, 3.4, 2.4, and 1.48 kyr cycles are the most prominent. Our results are in good agreement with other studies of Upper Triassic Lofer cyclic successions. The similarities in the thickness of individual Lofer cycles, the periods of all identified cycles, and the sedimentary rates suggest common allocyclic processes. Our findings provide definitive evidence for the orbital forcing of carbonate sedimentation in the Late Triassic Dachstein platform system. cyclostratigraphy astrochronology carbonate platform Dachstein Limestone Formation time-series analysis Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Introduction Thick Middle and Upper Triassic carbonate sequences deposited on the Western Neotethyan shelf commonly exhibit cyclic patterns and were the first subjects of early cyclostratigraphic analyses (Schwarzacher 1947, 1954; Fischer 1964): However, despite the long history of study, the origin of these carbonate cycles is still widely debated. The peritidal-subtidal Lofer cycles (Fischer 1964) were variously attributed to either allocyclic (Sander 1936; Schwarzacher 1954, 1993, 2005; Fischer 1964, 1975, 1991; Haas 1982, 1991, 1994; Schwarzacher and Haas 1986; Balog et al. 1997; Cozzi et al. 2005; Hinnov and Cozzi 2020) or autocyclic (Zankl 1967; Goldhammer et al. 1990; Satterley and Brander 1995; Satterley 1996; Enos and Samankassou 1998, 2021; Eberli 2013; Pollit et al. 2015; Samankassou and Enos 2019) processes. Although major advances have been made in the methodology of cyclostratigraphic analysis recently, the application of newly developed tools to the problem of Triassic carbonate cycles has remained limited (Hinnov and Cozzi 2020). During the Late Triassic kilometer-thick cyclic carbonate successions (Main Dolomite and Dachstein Limestone Formations) were deposited on the vast Dachstein platform system, located on the northwestern passive margin of the Neotethys Ocean. Meter-scale peritidal-subtidal cycles formed in the internal belt of these platforms were described and termed as Lofer cycles (Fischer 1964). Remnants of these platforms are exposed extensively in the Northern Calcareous Alps (e.g. Sander 1936; Fischer 1964), the Southern Alps (e.g. Bossellini 1967; Boselini and Hardie 1988), the Central and Inner Western Carpathians (e.g. Michalik 1980, 1993), the Transdanubian Range (e.g. Haas 1994, 2004), the Dinarides (e.g. Dimitrijevic and Dimitrijevic 1982, 1991), and the Hellenides (Pomoni-Papaioannou et al. 1986; Pomoni-Papaioannou 2008) and offer an excellent opportunity for a comparative study of the cyclic sequences. Here we present a detailed cyclostratigraphic analysis that employs the recently developed methodologies on the core Po-89 from the Bakony Mts. (Transdanubian Range, Hungary). The nearly complete lack of tectonic disturbances, the excellent recovery and preservation of the core, and the availability of previously recorded high-resolution datasets makes this core an exceptional candidate for a time-series analysis to tackle the long-standing issues about the Lofer cyclicity. Various macroscopically observed properties of the logged core section (lithology, colour and greyscale indices, and Lofer cycle member attribution) at a resolution of 10 cm are used to investigate the possible Milankovitch scale orbital forcing in the succession. We evaluate if orbital forcing also drove the detected variability of cycle completeness. Finally, we develop a depositional model that may explain the cyclic depositional processes and compare our results to all other available cyclostratigraphic data to assess the similarities and differences in the cyclic nature of the Dachstein Limestone and analogous formations. Geological setting The core Po-89 was drilled in 1979 near the village of Porva in the northern Bakony Mts. (Transdanubian Range, Hungary) (Fig. 1). The basal 33 m of the 408 m thick core section represents the uppermost part of the Fenyőfő Member, whereas the next 375 m belongs to the lower part of the overlying Dachstein Limestone Formation (Haas 1982). The Fenyőfő Member is a transitional unit between the typical Main Dolomite ( Fődolomit , Hauptdolomit , or Dolomia Principale in the Hungarian, German, and Italian literature, respectively) and Dachstein Limestone. Here, the subtidal C members of the Lofer cycles are not entirely dolomitised and the supratidal A members are better developed than in the Main Dolomite (Haas 2004; Haas et al. 2015). The entire core section is Norian in age based on its Megalodontaceae fauna and foraminifera assemblages (Haas 1982, 1995b) and is free of any observable tectonic disturbance (Haas 1982). The studied core section represents a part of the Upper Triassic platform carbonate succession of the Transdanubian Range Unit which was a segment of the vast Dachstein carbonate platform system developed on the passive margin of the Neotethys Ocean (Fig. 1) (Balla 1982; Haas 1987, 2004; Haas et al. 1990). In the Transdanubian Range the thickness of the Upper Carnian to Middle Norian Lofer cyclic Main Dolomite is ~800–1200 m, that of the transitional Fenyőfő Member is ~100–400 m, whereas the Upper Norian to Rhaetian Dachstein Limestone Formation is ~600–900 m thick (Haas 2004). In the Late Carnian the filling up of previously formed extensional basins led to a remarkably levelled topography and gave rise to the development of vast carbonate ramps/platforms. The Main Dolomite was deposited during the latest Carnian to mid-Norian under semi-arid climatic conditions, whereas increasing humidity during the Late Norian led to a gradual cessation of dolomitization (Balog et al. 1997; Haas 2004; Haas et al. 2015). The deposition of this carbonate sequence was terminated at the end of the Rhaetian, possibly in relation with the end-Triassic events (Pálfy et al. 2021). Dismemberment and subsequent drowning of most parts of the platform occurred near the Triassic-Jurassic boundary (Haas 1995a, b). During the Alpine orogeny the entire Transdanubian Range Unit was incorporated into the Alpine nappe system as part of the ALCAPA Megaunit but it remained unmetamorphosed and largely intact (Balla 1982; Haas 1987, 2004; Haas et al. 1990). Thus, the ~2 km thick Lofer cyclic carbonate sequence can be studied in this area across its entire thickness with little or no distortion. Methods Creation of the time-series The original core log was digitized (Supplementary Material S1) and four different time-series (Lofer cycle member attribution, colour, greyscale, and lithology) were generated using uniform 10 cm sample spacing (Fig. 2). Firstly, numbers were assigned to the standard facies types, i.e. members of the Lofer cycles (Fischer 1964), as follows: member A and A’ was marked with 1, member B and B’ was marked with 2, and member C was marked with 3. Secondly, the colour of the rock was also converted to numbers, keeping the order in the original dataset as follows: 1 – white, 2 – yellow, 3 – brown, 4 – red, 5 – green, 6 – grey, 7 – black. The original core description distinguished light, medium, and dark shades of the colours, except for the white and the black. This was indicated in the derived time-series as X.1 for a lighter shade, X.2 for a medium shade, and X.3 for a dark shade of colour X, where X is the number assigned to the base colour. Where two or more colours were indicated, we assigned their average value. Thirdly, as a more rigorous numeric approach, we assigned a greyscale value for all the colours and their different shades and used these values to create a greyscale time-series (Fig. S1). For a comparison of their performance, we calculated the correlation coefficients of the greyscale and colour time-series with the Lofer cyclicity and found that the greyscale record yields nearly four times higher correlation coefficients than the colours, thus more faithfully track the facies changes within Lofer cyclic series. The fourth time-series was created on the basis of lithology. The numeric values assigned to the different lithologies are summarized in Table 1. Where two or more types of lithology were indicated in the original log, their average value was used. All the generated time-series are provided in the Supplementary Material S2. Time-series analysis The cyclostratigraphic analyses were carried out using the Acycle software (v2.4) (Li et al. 2019). The data preparation for each time-series that yielded the best results and the detailed settings of some of the applied methods are provided and discussed in the Chapter 1.2 of the Supplementary Material S3. Power spectra were generated using zero-padding (Bloomfield 1976), F-test, and the Multi-taper Method (MTM) (Thomson 1982; Mann and Lees 1996). The confidence levels for the power spectra were generated using the robust autoregressive model (robust AR(1)) (Mann and Lees 1996). The evolutionary spectra were generated using the Fast Fourier transform (LAH) method (Kodama and Hinnov 2015). To match the detected cycles with the Milankovitch cycles, the ratio method was used, which compares the ratio of the periods of the detected cycles to the ratio of the known period of the Milankovitch cycles. In addition, the quantitatively more robust COCO, eCOCO (Li et al. 2019), and TimeOpt, as well as eTimeOpt (Meyers 2015) methods were also applied to all of the time-series. For filtering, a Gaussian bandpass filter was used (Kodama and Hinnov 2015) and Coherence and phase analysis was also carried out to decipher the relationship between the different time-series. Wavelet analysis (Torrence and Compo 1998) was also performed on the Lofer cyclicity, colour and greyscale index time-series using the Acycle (v2.2) software. Results Identification of cycles and their linking to Milankovitch cycles The cyclostratigraphic analysis reveals several spectral peaks (Table 2). The same cycles are found in all the analysed time-series (Fig. 3). However, the signal of some of the shortest cycles (with periods of less than 2 m) is affected by more noise, making their interpretation more difficult. Using the lithology time-series, the signal of the smaller cycles is weaker due to the inherently smaller variability. The clearest and most pronounced signals are detected for the cycles with periods of 32, 20, 13, 5.5, 4.5 and 3.6 m. Of these, the 13 and 3.6 m cycles are exceptionally robust in all the time-series. The largest cycle with a period of 66.6 m also displays a robust spectral peak but its frequency has a wider interval that causes its spectral power to be distributed, therefore it appears weaker. Frequency (cycle/m) Period (m) Periods of sedimentary cycles (kyr) The identified orbitally-forced cycles and their period 0.015 66.6 404 Long eccentricity (405 kyr) 0.031 32.26 195.5 ~200 kyr 0.05 20 121.2 Short eccentricity (125 kyr) 0.077 13 78.7 Short eccentricity (95 kyr) 0.141 7.1 42.9 Obliquity (42.7 kyr) 0.182 5.5 33.3 Obliquity (34.2 kyr) 0.223 4.5 27.2 Obliquity (26.1 kyr) 0.26 3.85 23.3 Obliquity (25.3 kyr) and/or precession (21.2 kyr) 0.28 3.6 21.65 Precession (21.2 kyr) 0.3465 2.9 17.5 Precession (17.5 kyr) 0.45 2.22 13.5 Semi/hemi-precession (~9–13 kyr) 0.635 1.575 9.5 Semi/hemi-precession (~9–13 kyr) 0.7 1.43 8.7 Semi/hemi-precession (~9–13 kyr) 0.78 1.28 7.77 Heinrich events (~7–8 kyr) 0.855 1.17 7.1 Heinrich events (~7–8 kyr) 1 1 6 ? 1.08 0.926 5.6 Heinrich events or harmonics of precession (~4–5 kyr) 1.17 0.85 5.2 Heinrich events or harmonics of precession (~4–5 kyr) 1.4 0.714 4.3 Heinrich events or harmonics of precession (~4–5 kyr) 1.77 0.565 3.4 Heinrich events or harmonics of precession (~4–5 kyr) 2.05 0.49 2.95 ? 2.22 0.45 2.73 ? 2.535 0.4 2.4 Hallstatt or Bray solar activity cycles (~2.3 kyr) 2.94 0.34 2.06 Hallstatt or Bray solar activity cycles (~2.3 kyr) 3.3 0.3 1.84 ? 3.53 0.283 1.72 ? 3.8 0.263 1.6 Dansgaard–Oeschger cycles (~1.3–1.6 kyr) 4.1 0.244 1.48 Dansgaard–Oeschger cycles (~1.3–1.6 kyr) 4.3 0.23 1.41 Dansgaard–Oeschger cycles (~1.3–1.6 kyr) Table 2 Matching of the detected periodicities with the Milankovitch cycles at a sedimentary rate of 16.5 cm/kyr. The cycles within the sub-Milankovitch range are shown below the double line. The periods of the Milankovitch cycles are based on the La2004 model for 218 Ma (Laskar et al. 2004). See text for a discussion of the periods of the sub-Milankovitch cycles To link the observed cycles with the Milankovitch cycles, determination of the sedimentary rate is of paramount importance. The COCO and eCOCO method yield a stable sedimentary rate of either ~3 or ~13–17 cm/kyr. However, the TimeOpt and eTimeOpt methods only support a stable sedimentary rate of c. 15 cm/kyr (Fig. 4). The lower, ~3 cm/kyr sedimentary rate is indeed unlikely, because in that case the ~2–3 m thick Lofer cycles in the Transdanubian Range (Haas 1982, 1994, 2004; Balog et al. 1997) would represent the ~100 kyr short eccentricity cycle, implying a more than 80 Myr duration for the deposition of the ~2 km thick Lofer cyclic carbonate sequence. However, independent stratigraphic constraints suggest that this succession is confined to only a part of the Late Triassic. A sedimentary rate around 15 cm/kyr would closely match the Lofer cycles with the precession cycles as suggested by earlier studies (Sander 1936; Schwarzacher 1954, 1993, 2005; Fischer 1964; Garrison and Fischer 1969; Schwarzacher and Haas 1986; Haas 1994; Balog et al. 1997; Cozzi et al. 2005; Hinnov and Cozzi 2020). Thus, having broadly established the most likely sedimentary rate as c. 15 cm/kyr, we used the ratio method to determine the sedimentary rate that would provide the best match between the ratios of the periods of the identified cycles and the Milankovitch cycles. The best result falls in the higher part of the range of possible sedimentary rates, at ~16.5 cm/kyr. Matching of the here identified cycles with the orbitally forced (i.e. Milankovitch and sub-Milankovitch) cycles is presented in Table 2. The match between the calculated periods of the identified cycles and the expected periods of the Milankovitch cycles (Laskar et al. 2004, 2011; Hinnov and Hilgen 2012) is exceptionally good for the Late Triassic, only the peculiar ~200 kyr cycle needs further consideration. Previously, any detected cycle in the ~200–250 kyr range was not regarded as a true orbital cycle. However, several recent studies suggest that indeed it may represent a real orbital cycle (e.g. Friedrich et al. 2008; Liebrand et al. 2016; Hilgen et al. 2015). Hilgen et al. (2020) suggested that this cycle either arises from the non-linear response to the astronomical forcing or, more likely, from the alternation of strong and weak ~100 kyr minima in short eccentricity. Alternatively, Huang et al. (2021) argued that a ~173 kyr cycle may result from obliquity forcing. Thus, although a ~200 kyr cycle may reflect orbital forcing in the sedimentary record, its origin remains debated. As the here studied Lofer cycles were formed at low paleolatitude, an eccentricity-related origin is more plausible. At the sub-Milankovitch scale, i.e. for periods less than ~17–20 kyr, the matching is more difficult in the lack of established target cycle periods. The most prominent sub-Milankovitch cycles found here are the 13.5, 3.4, 2.4, and 1.48 kyr cycles. In addition, noisier but still significant cycles occur with periods of 5 and 7 kyr. A detailed treatment of their possible origin is given in the relevant subsection of the Discussion. Duration of deposition recorded in the core Po-89 To determine the time of deposition recorded in the studied section of the core Po-89, the 405 kyr long eccentricity, the 95 kyr short eccentricity, the 34 kyr obliquity and the 21 kyr precession signals are filtered from all the time-series, then tuned to the respective cycles. The resulting duration consistently falls in the range of 2.42–2.58 Myr, with an average of 2.487 Myr. Thus, the studied core Po-89 represents an approximately 2.5 Myr interval of carbonate platform deposition within the Norian. Other observations from the cyclostratigraphic analysis The evolutionary spectra of the studied time-series consistently reveal three intervals with lower levels of spectral power (Fig. 5). These are as follows: from -94.4 m (top of the core) to -140 m, from -240 m to -330 m, and from -480 m to -502.1 m (bottom of the core). The first two likely result from the overall smaller variance in the time-series within these intervals, whereas the third interval entirely represents the partially dolomitized Fenyőfő Member. According to the wavelet analyses and the evolutionary spectra, along the more prominent erosional surfaces usually only the signal of the cycles with periods of less than 2 m is distorted (Fig. 6). However, there are two erosional surfaces (at -204 and -290 m) where the signal of the cycles with periods up to 4 m period is also distorted. Nonetheless, these observations suggest that the succession is most likely complete even at the level of the Lofer cycles (i.e. at the precession scale) and definitely undisturbed at the obliquity and eccentricity scale. Coherence and phase analyses reveal that the lighter colours and greyscale values consistently belong to the members C in the Lofer cycles, whereas the darker colours and greyscale values consistently belong to the members A. Members C also correspond to lower values of the lithological index, i.e. limestone or dolomite, whereas members A correspond to higher lithological index values, i.e. more argillaceous lithologies. These findings are in good agreement with the macroscopic observations. Discussion Cyclic depositional model The Upper Triassic Lofer cyclothems in the Northern Calcareous Alps and their elementary Lofer cycles were originally defined and described as unconformity-bounded, deepening-upward (i.e. transgressive) sedimentary cycles that are made up of three characteristic lithofacies types, referred to as Lofer cycle members A, B, and C (Fischer 1964). Member A consists of red or green marl or claystone that commonly contains pebble-sized clasts of penecontemporaneous limestone. Member B is characterized by stromatolites and/or fenestral laminites (loferites) with common occurrence of desiccation features. Member C is made up of carbonates with wackestone or packstone texture that contain shallow marine fossils, including locally abundant megalodontids and benthic foraminifera. Originally, members A and B were interpreted as tidal flat deposits that were formed in the supratidal and intertidal zones, respectively, whereas member C is characteristic to the subtidal zone (Fischer 1964). Subsequently, however, it was recognised that the ideal elementary Lofer cycle shows a symmetrical A-B-C-B’(-A’) pattern (Haas 1982). The regressive member B’ is similar to the transgressive member B but it is commonly mud-cracked, leached, and, in some cases, more intensely dolomitized (Haas 1982, 1994). The typical Lofer cyclic successions were deposited on the inner (i.e. more coastal) part of the platform, characterized with a very gently sloping (~1°) ramp-like topography. The adjacent outer platform had a slightly steeper slope, stabilized by primarily microbial, and subordinately metazoan mounds ("microbial reefs") and oncoidal mounds accumulated by vigorous currents. Thus, although typical Lofer cycles did not form on the outer part of the platform system, nevertheless the outer platform could also influence the deposition on the inner platform via the so-called basket effect (Haas 1994, 2004). During a lowstand, large areas of the inner platform become subaerially exposed and are subjected to karstification and pedogenic processes, while most of the outer platform remains submerged. At the onset of the transgression, as the sea level starts to rise and reaches the inner platform, first the terrestrial sediments and the erosional products are reworked and redeposited (member A). Subsequently, if the sea level rise is slow, a microbial mat-covered tidal flat environment is established (member B). In this scenario, there is no basket effect and the platform behaves as a ramp-like platform, leading to the development of an ideal Lofer cycle. On the contrary, when the basket effect applies and/or the sea level rise is too rapid, most of the inner platform immediately transitions into the subtidal zone where member C is deposited. This model may explain the occasionally missing A and/or B members. After reaching the maximum flooding, during the late highstand, normal regression occurs and, with the reduction of the available accommodation space, the inner platform transitions into a tidal flat covered by microbial mats again (member B’). If this process is too fast, member B’ may be missing entirely. In both cases, however, member B’ could also be removed by erosion, when forced regression takes place and the inner platform becomes subaerially exposed again at the end of the sequence. This leads to the development of a disconformity, occasionally with the presence of member A’ (Haas 1982, 1994, 2004). These cyclic sea level fluctuations are hypothesized to be of a few metres to 15 m in amplitude (Fischer 1964; Haas 1994; Balog et al. 1997) and commonly associated with orbitally forced eustatic sea-level variations (Sander 1936; Schwarzacher 1954, 1993, 2005; Fischer 1964, 1975, 1991; Haas 1982, 1991, 1994; Schwarzacher and Haas 1986; Balog et al. 1997; Cozzi et al. 2005; Hinnov and Cozzi 2020). From the Late Carnian to the Rhaetian, the Dachstein platform was not affected by any significant tectonic deformation and only a prolonged, slow and gradually accelerating subsidence is assumed (Haas 1994). Previously, the thermal expansion of sea water was hypothesized as the most likely driving force of orbitally-driven sea-level fluctuations during greenhouse climate states, supported by modeling that showed that this process can generate sea level variations up to 2 m (Schulz and Schäfer-Neth 1997). More recently, however, aquifer- and limno-eustasy is increasingly accepted as a more potent driving force as several studies suggested that the water-bearing potential of groundwater aquifers and lakes in greenhouse climate state is about equal to that of polar ice caps during icehouse intervals (Southam and Hay 1981; Hay and Leslie 1990; Wagreich et al. 2014; Peters and Husson 2015; Wendler et al. 2016). Aquifer- and limno-eustasy continuously redistributes water between the oceans and continents. During the maximum of seasonality, the hydrological cycle strengthens, and water is delivered from the oceans to the continents via precipitation. The continental surface and subsurface reservoirs such as lakes and groundwater aquifers recharge, the water levels of the lakes rise while, at the same time, the global sea level falls. During the minimum of seasonality, the hydrological cycle weakens, and the continental reservoirs discharge via fluvial runoff. This would lead to a lowering of water level in lakes and concomitant sea level rise (Wagreich et al. 2014; Li et al. 2016; Wendler et al. 2016; Li et al. 2018). Several recent studies document the antiphase relationship between variations of sea level and lake water levels linked by orbital forcing in the Mesozoic (e.g. Wagreich et al. 2014; Li et al. 2018). One such study is especially relevant as it demonstrated the relationship between sea level variations observed in Lofer cycles in the Southern Alps and lake level variations in the Newark Basin (Hinnov and Cozzi 2020). In addition, ˝megamonsoon˝-driven aquifer- and limno-eustasy is proposed from the partly coeval intraplatform Csővár basin that was located on the outer part of the Dachstein platform system in the Transdanubian Range (Vallner et al. 2023). Our analysis of the core Po-89 reveals that the thickest members C were deposited consistently during long eccentricity minima, when the climate was more balanced, and seasonality could reach its absolute minima. This finding is in agreement with the concept of aquifer- and limno-eustasy that predicts that the long eccentricity minima are associated with generally higher sea level and increased accommodation space, promoting the deposition of thick members C. In the opposite phase, during the long eccentricity maxima, although conditions may favour the formation of members A, they do not become thicker or more common in the record. As member A is pedogenic and redeposited in origin and prone to erosion, this observation does not contradict the model of aquifer- and limno-eustatic control. Orbital forcing on the completeness of the Lofer cycles The common occurrence of symmetrical A-B-C-B’(-A’) Lofer cycles was first described from the core Po-89, but incomplete cycles with depositionally missing members and/or truncated cycles that were affected by a higher degree of subaerial erosion were also encountered (Haas 1982). This observation raises the possibility of orbital forcing of the different completeness of the cycles preserved in the sedimentary record. To test this hypothesis in general, and to assess if the dominant cycle types and average cycle completeness differs at long eccentricity minima and maxima, here we apply time-series analysis on the cycle completeness. First, a completeness index was developed to categorize each cycle, based on the subdivision described by Haas (1998) (Table 3). Then, time-series analysis was carried out using the same data preparation steps and settings for the power and evolutionary spectra generation as for the analyses of other time-series. Index value Description Cycle types 1 Ideal, symmetric, complete cycles dABCB'A'd; dABCB'd 2 Incomplete cycles with depositionally missing members dBA'd; dCB'd; dCA'd; dBCB'd; dACB'd; dABCA'd 3 Truncated cycles with higher degree of subaerial erosion at their top dABCd 4 Incomplete and truncated cycles dACd; dCd Table 3 Completeness index used to test the possible orbital forcing of the different completeness of the Lofer cycles. d – disconformity, i.e. erosion between the different cycle members We found that during the long eccentricity maxima the average of the completeness indices of the cycles was consistently lower than during long eccentricity minima, with only one exception (at a long eccentricity minimum between -147 and -177 m). The average value of all long eccentricity maxima is 1.5, in stark contrast to the average of 2.7 of all long eccentricity minima. The complete, symmetrical cycles are more common during the maxima, whereas the minima are dominated by the incomplete and truncated cycle type. The purely incomplete and purely truncated Lofer cycle types do not dominate any orbital cycle segments; they are nearly evenly distributed along the long eccentricity curve (Fig. 7). The results of the time-series analysis of the completeness index are noisier but they are in agreement with the other time-series analyses performed. However, due to the lower resolution of the completeness index, the majority of the sub-Milankovitch cycles are not detectable by this method (Fig. 8). Our results imply that the different completeness of the Lofer cycles is also driven by Milankovitch-scale orbital forcing, possibly through the changing pace of sea level variations controlled by the available water mass in the oceans. As a consequence of aquifer- and limno-eustasy, long eccentricity maxima are associated with less available water mass in the oceans and thus generally lower sea level. As a result, slower changes of sea level are expected that, together with the effect of lower sea level, would lead to a complete development of each facies types within the Lofer cycle. On the contrary, during long eccentricity minima, when the available water mass is greater, the sea level is generally higher, and subsequently the sea level changes are faster, the inner platform would remain mostly in the subtidal zone and enter the intertidal zone for only a short period of time that is insufficient for the members B and B’ to develop properly. In this case, commonly only a disconformity surface is formed that marks a brief subaerial exposure. These conditions also explain the detected higher thickness of members C during long eccentricity minima. The time-series analysis of the completeness index revealed another peculiar phenomenon. A comparison of the evolutionary spectra (Fig. S2) allows the identification of three segments (from -94.4 m to -140 m, -240 m to -330 m, and -480 m to 502.1 m, respectively) where the original time-series yields lower levels of spectral power, as opposed to the higher levels of spectral power in the completeness index time-series. On the contrary, all other segments with higher levels of spectral power in the original time-series are found to exhibit less spectral power in the completeness index time-series. A plausible explanation of this antiphase relationship calls for oppositely changing variance in the original time-series and the completeness index time-series. Thus, when the variability among the different cycle types is higher, i.e. more types are alternating more frequently, then the variability within the Lofer facies types is lower. Then, fewer facies types and a more limited range of lithology, colour, and greyscale values are alternating, and do so with a lower frequency. The changing variability among these segments exhibited by the completeness index time-series is also apparent in Fig. 7. We suggest that this pattern stems from the inherent properties of the genesis and preservation of Lofer cycles. The maximum variance in the Lofer facies types, as also reflected in the broadest range of lithology, colour, and greyscale indices, occurs when most of the Lofer cycles are complete and there is only limited deviation from the ideal type, i.e. minimal variance among the cycle types. It follows that changes in variance may also be paced by the orbital cycles as the dominance of the complete cycle type is proved to be controlled by the long eccentricity cycle. Since there are only three complete segments of higher and lower variability within the core, time-series analysis cannot offer a rigorous test for this hypothesis, yet the similar thicknesses of these segments may still hint at regular cyclicity. The thickness of these segments is 100, 90, and 150 m, respectively, which may form parts of larger cycles with periods of 190–240 metres. Notably, Schwarzacher (2005) also reported the presence of 190–240 m thick cycles from the bundles of Lofer cycles in the Leoganger Steinberge section in the Northern Calcareous Alps. A conversion of the thickness of this, as yet hypothetical cycle to time domain, using a sedimentary rate of 16.5 cm/kyr as determined in this study, yields a period of 1.15–1.45 Myr. Remarkably, there is a striking coincidence of this period with that of the ~1.2–1.3 Myr grand orbital cycle (Lourens and Hilgen 1997; Li et al. 2018; Boulila 2019), pointing to another level in the hierarchy of orbital control exhibited in Lofer cyclic successions. Sub-Milankovitch cycles Another notable outcome of our cyclostratigraphic analyses is the identification of 19 cycles in the sub-Milankovitch band, i.e. with periods of less than ~17–20 kyr (Table 2). The most prominent among them are the cycles of 13.5, 7, 5, 3.4, 2.4, and 1.48 kyr. Currently there are no established target cycles for the Mesozoic in this scale, which makes their matching to known cycles challenging. However, several recently published cyclostratigraphic studies report sub-Milankovitch cycles from the Mesozoic, therefore a comparison with their results may provide further insights, despite the lack of agreement on the driving forces of these cycles. The most characteristic sub-Milankovitch cycles identified in other studies for the Mesozoic are the cycles of ~9–13, ~7–8, ~4–5, and ~1.5–2 kyr (Rodríguez-Tovar and Pardo-Igúzquiza 2003; Zühlke et al. 2003; Kent et al. 2004; Friedrich et al. 2005; Vollmer et al. 2008; Boulila et al. 2010; Wu et al. 2012; De Winter et al. 2014; Chu et al. 2020; Boulila et al. 2022; Hasegawa et al. 2022; Ma et al. 2022; Zhang et al. 2023a). Several recent studies propose a link of the ~9–13 kyr cycle with the so-called hemi- or semi-precession cycle (Rodríguez-Tovar and Pardo-Igúzquiza 2003; Vollmer et al. 2008; Wu et al. 2012; Chu et al. 2020; Zhang et al. 2023a). Theoretically, a cycle with half the period of the precession may arise from the insolation maxima due to the biannual passage of the Sun across the intertropical zone (Berger and Loutre 1997; Berger et al. 2006). In the context of the present study, however, an alternative explanation, that these cycles may arise from the occurrence of incomplete or truncated Lofer cycles, cannot be ruled out. The ~7–8 kyr cycle was linked to the Heinrich events (e.g. De Winter et al. 2014), even though the Heinrich events were originally described from the last glacial period and are thought to correspond to ice sheet melting (Heinrich 1988). However, recent studies suggest that this cycle may originate in the tropical areas, as the nonlinear response to precession-induced insolation variations and subsequent changes in El Niño frequency (e.g. Turner 2004; Ziegler 2009). The the ~4–5 kyr cycles are also linked to either the Heinrich events (Hasegawa et al. 2022) or the harmonics of the precession (Chu et al. 2020), whereas the ~1.5–2 kyr cycles are associated with either the 1.3–1.6 kyr Dansgaard–Oeschger (DO) cycles modulated by the precession cycle and its harmonics (Boulila et al. 2022; Hasegawa et al. 2022) or the ~1 kyr Eddy and ~2.3 kyr Hallstatt or Bray solar activity cycles (Hasegawa et al. 2022; Ma et al. 2022). The DO cycles were originally described from records of the last glacial period (Dansgaard et al. 1982) but recent studies also established the presence of a cycle with similar period in the Mesozoic (Boulila et al. 2022; Hasegawa et al. 2022; Ma et al. 2022). Moreover, the controversial Latemar couplets also appear associated with a ~1.7–2.2 kyr cycle (Kent et al. 2004). Our results provide additional support to the conclusions of the studies cited above, as we suggest that the 8.7–13.5 kyr cycles likely represent the semi/hemi-precession cycles, the 7.1–7.77 kyr cycles the Heinrich events, the 3.4–5.6 kyr cycles also the Heinrich events or harmonics of the precession cycle, the 2.06–2.4 kyr cycles the Hallstatt or Bray solar activity cycles, and the 1.4–1.6 kyr cycles the DO cycles (Table 2). However, to explain the origin of the 1.72–1.84, 2.73–2.95, and 6 kyr cycles remains challenging. Tentatively we propose that the 1.72–1.84 kyr and 2.73–2.95 kyr cycles may be similar to the Latemar couplets with an as yet unknown driving force or, alternatively, may be related to either the DO cycles or solar activity cycles, whereas the 6 kyr cycle may represent another expression of the Heinrich events or harmonics of the precession. Comparison with other Lofer cyclic successions As the allocyclic vs autocyclic nature of the Lofer cyclothems has long been debated, a regional comparison is warranted and may yield additional insights. From the Alps to the Hellenids, we comprehensively collected the available data on the thickness of the individual Lofer cycles, the thickness and proposed period of the other identified cycles, and sedimentary rates within the Lofer cyclic successions (Table 4). To validate the hypothesis of orbital forcing, a high degree of similarity in the cyclic pattern of geographically distant study areas is expected. Reference Location of the studied section(s) Thickness of an individual Lofer cycle Identified cycles Calculated sedimentary rate Method(s) used Schwarzacher (1954) Loferer Steinberge, Northern Calcareous Alps, Austria average 3.5 m 3.5 m (~20 kyr) & 15–18 m (~100 kyr) — suggested by bundling pattern Fischer (1964) Dachstein, Leoganger Steinberge, Steinernes Meer & Loferer Steinberge sections, Northern Calcareous Alps, Austria 5–6 m ~20, 50 & 100 kyr ~11 cm/kyr* thickness divided by time & Fischer-plot Schwarzacher and Haas (1986) Loferer Steinberge, Steinernes Meer & Dachstein sections, Northern Calcareous Alps, Austria and cores T-5, Po-89 & Ut-8, Transdanubian Range, Hungary average 3.5 m (Loferer Steinberge), 5.69 m (Steinernes Meer), 4.84 m (Dachstein), 2.21 m (T-5 core), 3.1 m (Po-89 core) & 4.29 m (Ut-8 core) 2.5–4 m (~20 kyr), 5–7 m (~40–45 kyr), 12–15 m (~100 kyr), 20–27 m (~150–200 kyr) & 45 m (~300 kyr) ~13–23 cm/kyr, most likely within 13.3–16.5 cm/kyr thickness divided by time, Fischer-plot & Walsh power spectra on Lofer ABC indices from the Loferer Steinberge and the Hungarian core sections Haas (1982, 1994, 2004) Transdanubian Range 2–5 m, average 3.1 m — ~15–16 cm/kyr thickness divided by time Balog et al. (1997) Cores Ut-8, Zt-62, E-5, T-5, Td-4 & Po-89, Transdanubian Range, Hungary 1–5 m, average 3.1 m 2–3 m (~20 kyr), 5–7 m (~35–45 kyr), 12–14 m (~90–100 kyr), 33 m, 40–50 m (~400 kyr) & 99 m ~10–16 cm/kyr thickness divided by time, Fischer-plot on cores Ut-8, Po-89, T-5, Zt-62 & Td-4 & Walsh and Fast Fourier Transform (FFT) power spectra on Lofer ABC indices from core Po-89 Cozzi et al. (2005) Monte Canin section, Julian Alps, Italy average 2.41 m 1.6–3.5 m (~20 kyr), 13.7 m (~100 kyr) & 54 m (~400 kyr) ~8–18 cm/kyr* multiple power spectra and evolutionary spectra on greyscale indices created from field photographs Schwarzacher (2005) Loferer Steinberge, Leoganger Steinberge & Steinernes Meer sections, Northern Calcareous Alps, Austria 2–3.5 m 2–3.5 m (~20 kyr), 5–7 m, 9–13 m, 15–27 m (~100 kyr), 60–80 m (~400 kyr), 190–240 m ~15–20 cm/kyr Lomb-Scargle analysis on greyscale indices created from field photographs from the Leoganger Steinberge Haas and Pomoni-Papaioannou (2009) Argolis Peninsula, Hellenids, Greece 1–5 m — — — Todaro et al. (2017) Monte Sparagio section, Sicily, Italy 0.8–3 m — — — Hinnov and Cozzi (2020) Monte Canin section, Julian Alps, Italy average 2.41 m 2–3.1 m (~17–23 kyr), 4.46–8.3 m (~30–50 kyr), 17.3 m (~100 kyr) & 21.3–39.5 m (~400 kyr) ~15–17 cm/kyr MTM power spectra, FFT evolutionary spectra, and tune and release method on the data from Cozzi et al. (2005) This study Core Po-89, Transdanubian Range, Hungary average 3.1 m 2.9–3.6 m (~17.5–21.6 kyr), 3.85–7.1 m (~23.3–42.9 kyr), 13–20 m (~78.7–121.2 kyr), 32.3 m (~200 kyr) & 66.6 m (~404 kyr) ~16.5 cm/kyr See Chapter 3 Table 4 Summary of published cyclostratigraphic analyses of Lofer cyclic successions, with the estimated thickness of individual Lofer cycles, detected periods and their matching with orbital cycles, calculated sedimentary rates, and the method(s) used in each study. If the sedimentary rate was not given in the original study, it is calculated here (denoted by an asterisk) from the known and matched periods of the detected cycles The thickness of the Lofer cycles consistently falls between 1 and 6 m, with an average thickness of 2.5–3.5 m, whereas the inferred sedimentary rate is also consistent between 10 and 20 cm/kyr. Most studies suggest the precession cycle as the driving force for the basic cycle, in accordance with the earlier assumption (Sander 1936; Fischer 1991; Schwarzacher 1993), except one study that suggested obliquity forcing, although based on limited data only (Fischer 1964). Each study that was based on detailed cyclostratigraphic analysis successfully identified the short and long eccentricity cycles with periods of ~12–17 m and ~50–70 m, respectively, whereas five out of six studies also found cycles in the frequency band of obliquity (with periods between ~4–7 m) and a cycle with a ~30 m period. The similarity between the periods is remarkable. All the studies reported a robust short eccentricity signal exhibited in the bundling pattern of the individual Lofer cycles, whereas the long eccentricity signal appears weaker, more fragmented, distorted, or ambiguous. The latter finding is consistent with the observation of less clear and obvious 20:1 bundling pattern of the Lofer cycles (Haas 1982; Haas and Schwarzacher 1986; Goldhammer et al. 1990; Balog et al. 1997). These similarities among sections in the Northern Calcareous Alps, the Transdanubian Range, the Southern Alps, Sicily, and the Hellenids imply that regular cyclicity was not an isolated phenomenon but rather a prevalent depositional feature in the entire Dachstein platform system (Fig. 9). Consequently, Milankovitch-scale orbitally forced eustatic sea level variations remain the only plausible cause for the near-uniform cyclicity that affected such a broad paleogeographic area for an extended period of time. Although the local effect of autocyclic processes on the sedimentation cannot be ruled out entirely, their role was much more limited. Most of the studies that question the orbital forcing present arguments that the Lofer cycles have lateral thickness variations, occasionally they pinch out, and many cycles are not complete (Satterley and Brander 1995; Enos and Samankassou 1998, 2021; Samankassou and Enos 2019). In addition, questions were raised about the consistency of the stacking pattern and the viability of a driving force in a greenhouse world (Goldhammer et al. 1990; Satterley and Brander 1995; Satterley 1996). To fend off these criticisms, it was pointed out that lateral variability was observed only in the Steinerness Meer section but elsewhere, in other sections studied in the Northern Calcareous Alps, lateral variations are rather rare (Schwarzacher 2005). Concerns of the consistency of stacking pattern were based solely on visual observation or Fischer-plots, rather than on detailed cyclostratigraphical analysis (Schwarzacher 2005). Although the core Po-89 used in this study obviously does not afford an opportunity to examine lateral variations, it is eminently suitable to detect orbital forcing due to the exceptional preservation of the cycles. As demonstrated in Table 4, our results are coherent with the other, originally distant parts of the Dachstein platform system (Fig. 9). It is not conceivable that random processes would produce highly similar, hierarchical sedimentary cyclicity across a wide geographic area and through an interval of millions of years, such as the spatial and temporal extent of the Dachstein platform system. The credibility of our results obtained using up to date cyclostratigraphic tools is also supported by the demonstration of the reliability and sensitivity of this methodology (Sinnesael et al. 2019). An independent line of supporting arguments is provided by studies of the Upper Triassic to lowermost Jurassic carbonates deposited in the peri- and intraplatform basins of the Dachstein platform system. These deposits consist of calciturbidites that were sourced primarily from the adjacent platforms (Vallner et al. 2023). As Milankovitch cyclicity was identified in several of these deposits (Mesetti et al. 1989; Reijmer and Everaars 1991; Reijmer et al. 1993; Maurer et al. 2004; Vallner et al. 2023), it is highly likely that the deposition in the platforms and the adjacent basins were both paced by the same orbital cycles. Our discussion of the results of this study is intended to help to settle the debate that has been going on for more than 70 years. The definitive evidence for orbital forcing of the sedimentation in the Late Triassic platforms validates the use of cyclostratigraphy and astrochronology as high-resolution stratigraphic tools for the Dachstein Limestone Formation and its analogues. In addition, comparison of the Upper Triassic cyclothems with the younger platform deposits that record orbitally forced cycles, as in the Arabian and the Adriatic Platforms, will further our understanding of the general patterns of cyclic sedimentation in the Mesozoic carbonate platform environments. Conclusions 1) The detailed archive log of a more than 400 m thick record of the cyclic Norian Dachstein Limestone in the Po-89 core was suitable to produce a high-resolution time-series of Lofer facies type, colour, greyscale, and lithology at 10 cm sample spacing. 2) Cyclostratigraphic analysis successfully revealed several spectral peaks that could be confidently matched with the Milankovitch cycles. Cycles with a period of 3.6 m are especially robust and represent the elementary Lofer cycles that correspond to orbital precession cycles with a period 21.65 kyr. 3) The sedimentary rate is determined as 16.5 cm/kyr, thus the studied section in the core Po-89 represents 2.5 Myr of carbonate platform evolution. 4) Using the results of the cyclostratigraphic analysis, we developed a refined model of cyclic carbonate deposition in the Late Triassic Dachstein platform and demonstrated that aquifer- and limno-eustasy are the most likely drivers of cyclic sea level changes that transcribed the orbitally driven climate changes into the sedimentary record. 5) Variations in the genesis and preservation of the Lofer cycles led to differences in their completeness, resulting in complete, depositionally incomplete, erosionally truncated, and incomplete and truncated types. We show here, for the first time, that cycle completeness is also orbitally controlled and is especially sensitive to long eccentricity forcing. An additional, tentative but intriguing observation is that changes in the variance in cycle types may be paced by the 1.2–1.3 Myr grand orbital cycle. 6) The spectral analysis also revealed several sub-Milankovitch cycles, of which the 13.5, 7, 5, 3.4, 2.4, and 1.48 kyr cycles are the most prominent. We discuss their possible driving forces and support the views that many of the sub-Milankovitch cycles that were originally discovered in the Quaternary records could also be detected in the Mesozoic, despite the contrast between icehouse and greenhouse climate regimes. 7) Comparison with other studies of Upper Triassic Lofer cyclic successions from the extensive Dachstein platform system points to close similarities in the thickness of individual Lofer cycles, the periods of all identified cycles, and the sedimentary rates, that points to common allocyclic processes. Taken together, these findings provide definitive evidence for the orbital forcing of carbonate sedimentation in the Late Triassic Dachstein platform system. Declarations Acknowledgements We thank Dorottya Dénes for digitizing the original core log and Ádám Kocsis for providing a paleogeographic base map. This study was supported by the ÚNKP-23-3 New National Excellence Program of the Ministry for Culture and Innovation from the source of the National Research, Development and Innovation Fund to ZV and by the National Research, Development and Innovation Fund Grant K135309 to JP. Funding This study was supported by the ÚNKP-23-3 New National Excellence Program of the Ministry for Culture and Innovation from the source of the National Research, Development and Innovation Fund to ZV and by the National Research, Development and Innovation Fund Grant K135309 to JP. Competing interests The authors have no competing interests to declare that are relevant to the content of this article. 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ZÜHLKE, R., BECHSTÄDT, T. & MUNDIL, R. 2003: Sub-Milankovitch and Milankovitch forcing on a model Mesozoic carbonate platform - the Latemar (Middle Triassic, Italy). — Terra Nova 15, 69–80. https://doi.org/10.1046/j.1365-3121.2003.00366.x Supplementary Files SupplementaryMaterialS1.tif SupplementaryMaterialS2.xlsx SupplementaryMaterialS3.pdf Cite Share Download PDF Status: Published Journal Publication published 26 Oct, 2025 Read the published version in Palaeogeography, Palaeoclimatology, Palaeoecology → Version 1 posted You are reading this latest preprint version Research Square lets you share your work early, gain feedback from the community, and start making changes to your manuscript prior to peer review in a journal. As a division of Research Square Company, we’re committed to making research communication faster, fairer, and more useful. We do this by developing innovative software and high quality services for the global research community. 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Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-4281587","acceptedTermsAndConditions":true,"allowDirectSubmit":true,"archivedVersions":[],"articleType":"Research Article","associatedPublications":[],"authors":[{"id":294575586,"identity":"dbcf29e5-abf8-459b-b23a-9b0f1ddba9bc","order_by":0,"name":"Zsolt Vallner","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAA8klEQVRIiWNgGAWjYHACxgMgko8dRFYAMTNzA0E9B0B62JhBzDMgLYykaGFsA1uLX4t8/+EDhz8wHJZnY+Y9+LhyXm00fztQy4+KbTi1MM5ISwDactiwjZkv2fDstuO5Mw4zNjD2nLmNUwuzBI8BUEsaYxszj5lk47ZjuQ1ALcyMbbi1sPGfAWuxB2ox/9k451jufEJaeBhyQFpsEkG2MDY21ORuIKRFQgLolzMGNslALcaSDccO5G4EajmIzy/AEDv4oKJCwrafvcfwY0NNXe6880CRHxW4tUCAAZx1GEweIKAeBdSRongUjIJRMApGCAAAq3hXKahQsygAAAAASUVORK5CYII=","orcid":"https://orcid.org/0000-0002-6060-061X","institution":"Eötvös Loránd University: Eotvos Lorand Tudomanyegyetem","correspondingAuthor":true,"prefix":"","firstName":"Zsolt","middleName":"","lastName":"Vallner","suffix":""},{"id":294575587,"identity":"254a8896-827e-4cc8-a8d0-13030e6ac346","order_by":1,"name":"János Haas","email":"","orcid":"","institution":"Eötvös Loránd University: Eotvos Lorand Tudomanyegyetem","correspondingAuthor":false,"prefix":"","firstName":"János","middleName":"","lastName":"Haas","suffix":""},{"id":294575588,"identity":"354e224c-8e74-4924-8eae-85f86e0e8ff8","order_by":2,"name":"József Pálfy","email":"","orcid":"","institution":"Eötvös Loránd University: Eotvos Lorand Tudomanyegyetem","correspondingAuthor":false,"prefix":"","firstName":"József","middleName":"","lastName":"Pálfy","suffix":""}],"badges":[],"createdAt":"2024-04-17 11:29:45","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-4281587/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-4281587/v1","draftVersion":[],"editorialEvents":[{"content":"https://doi.org/10.1016/j.palaeo.2025.113365","type":"published","date":"2025-10-27T00:00:00+00:00"}],"editorialNote":"","failedWorkflow":false,"files":[{"id":55628794,"identity":"7cdf51c2-f1a4-4bf8-be81-ded6d469964e","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":771958,"visible":true,"origin":"","legend":"\u003cp\u003eLocation of the Transdanubian Range and adjacent areas in the Neotethyan shelf during the Norian (marked by a red rectangle on A and B) and the Po-89 core in the Transdanubian Range today (marked by a red dot on C). CAMP: Central Atlantic Magmatic Province, LBM: London-Brabant Massif, BM: Bohemian Massif, MM: Malopolska Massif, AA: Austroalpine Units, WC: Central and Inner West Carpathian Units, TI: Tisza Unit, TR: Transdanubian Range, SL: Slovenian basin, JU: Julian Alps, B: Bükk Unit, ADCP: Adriatic-Dinaridic Carbonate Platform, BO: Bosnian Zone, D: Drina–Ivanjica Unit, J: Jadar Block, SI: Sicilian Basin, L: Lagonegro Basin, JEF: Jefra Basin, PI: Pindos Basin, PEL: Pelagonian-Subpelagonian Units. Adapted from Haas and Pomoni-Papaioannou (2009), Kovács et al. (2020) and Kocsis and Scotese (2021)\u003c/p\u003e","description":"","filename":"Fig1.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/fa7776d91f7ccf446a69bac7.png"},{"id":55628796,"identity":"047d9842-6e1e-4801-9333-d09598feb136","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":250841,"visible":true,"origin":"","legend":"\u003cp\u003eLog of the core Po-89 showing the standard Lofer facies types and the colour, greyscale, and lithology index time-series\u003c/p\u003e","description":"","filename":"Fig2.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/dc19460b168f558a7aadc698.png"},{"id":55628799,"identity":"fcde8465-7dc0-473e-9d71-8978de56afd1","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":1558996,"visible":true,"origin":"","legend":"\u003cp\u003eInterpreted power spectra of the Lofer cyclicity (A), greyscale index (B), lithology index (C) and colour index (D) time-series. The power spectra were cut at 2.5 cycles/m frequency due to resolution issues\u003c/p\u003e","description":"","filename":"Fig3.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/4ddb4530ba35bd0730ff48fb.png"},{"id":55628798,"identity":"ef322fe7-4199-4661-a274-c6ed96dc8b96","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":1952797,"visible":true,"origin":"","legend":"\u003cp\u003eResults of the TimeOpt (A) and eTimeOpt (B) methods applied to the Lofer cyclicity time-series\u003c/p\u003e","description":"","filename":"Fig4.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/322a2cc62b2ada92d40087e6.png"},{"id":55629551,"identity":"8629a569-9e44-4cb6-bc49-565f6cbd1834","added_by":"auto","created_at":"2024-04-30 19:10:16","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":3626972,"visible":true,"origin":"","legend":"\u003cp\u003eInterpreted evolutionary spectrum of the Lofer cyclicity time-series. The three intervals with lower levels of spectral power are marked with red rectangles. The evolutionary spectra were cut at 1.7 cycles/m frequency due to resolution issues\u003c/p\u003e","description":"","filename":"Fig5.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/57795cec310181679d0fc88e.png"},{"id":55628802,"identity":"204b3633-36f3-4911-a309-fcb890fa9a55","added_by":"auto","created_at":"2024-04-30 19:02:17","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":913658,"visible":true,"origin":"","legend":"\u003cp\u003eResult of the wavelet analysis applied to the Lofer cyclicity time-series. Note the continuity of the wavelet spectra above the period of two metres (black line).\u003c/p\u003e","description":"","filename":"Fig6.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/8de1f011e2b3cbdc9d8f4e7e.png"},{"id":55628801,"identity":"8764134e-0196-4a6c-82b8-e8946fe18124","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":70431,"visible":true,"origin":"","legend":"\u003cp\u003eThe completeness index with the filtered long eccentricity signal (red curve). The segments with higher variability (i.e. higher level of spectral power) are marked with red and those with less variability (i.e. lower level of spectral power) are marked with blue\u003c/p\u003e","description":"","filename":"Fig7.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/0c6463a0549c94cf7d466678.png"},{"id":55628804,"identity":"caec3a4c-8ad2-4140-873c-6789032ea92f","added_by":"auto","created_at":"2024-04-30 19:02:17","extension":"png","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":182645,"visible":true,"origin":"","legend":"\u003cp\u003eInterpreted power spectrum of the completeness index time-series. The power spectrum was cut at 0.5 cycles/m frequency due to resolution issues\u003c/p\u003e","description":"","filename":"Fig8.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/718bc1189cb401409d587531.png"},{"id":55628803,"identity":"4f31f180-7b6a-460e-8c80-c4f3cfbc77b4","added_by":"auto","created_at":"2024-04-30 19:02:17","extension":"png","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":207423,"visible":true,"origin":"","legend":"\u003cp\u003eLocation of the studied areas listed in Table 4 during the Norian. The base map was generated using the ˝chromosphere˝ package in R (Kocsis and Raja 2023) and the paleocoordinates of the studied areas were calculated from present-day coordinates for 220 Ma using the ˝rgplates˝ package in R (Kocsis et al. 2024)\u003c/p\u003e","description":"","filename":"Fig9.png","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/13256cceb908ca24e7a02da8.png"},{"id":97737689,"identity":"4b64cde5-8d13-4b40-b403-2bdd3e622ded","added_by":"auto","created_at":"2025-12-08 20:09:01","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":12893919,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/3e94b52e-414a-4018-bbec-82970e7217db.pdf"},{"id":55628882,"identity":"3324b63f-eaaf-476e-9147-4b170da5e5ab","added_by":"auto","created_at":"2024-04-30 19:02:45","extension":"tif","order_by":1,"title":"","display":"","copyAsset":false,"role":"supplement","size":437794436,"visible":true,"origin":"","legend":"","description":"","filename":"SupplementaryMaterialS1.tif","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/5e25e0584c82b5a329a5a050.tif"},{"id":55628795,"identity":"74f047fd-b379-4908-b4f8-543ce99e47d7","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"xlsx","order_by":2,"title":"","display":"","copyAsset":false,"role":"supplement","size":135742,"visible":true,"origin":"","legend":"","description":"","filename":"SupplementaryMaterialS2.xlsx","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/191476c907783d34633e5427.xlsx"},{"id":55628800,"identity":"309eb015-0100-4f1f-bc7f-9e10cfd266e2","added_by":"auto","created_at":"2024-04-30 19:02:16","extension":"pdf","order_by":3,"title":"","display":"","copyAsset":false,"role":"supplement","size":341580,"visible":true,"origin":"","legend":"","description":"","filename":"SupplementaryMaterialS3.pdf","url":"https://assets-eu.researchsquare.com/files/rs-4281587/v1/8eb47154dcaaeca4a1f14717.pdf"}],"financialInterests":"","formattedTitle":"Definitive orbital control on the origin and preservation of Lofer cyclicity in the Late Triassic Dachstein platform","fulltext":[{"header":"Introduction","content":"\u003cp\u003eThick Middle and Upper Triassic carbonate sequences deposited on the Western Neotethyan shelf commonly exhibit cyclic patterns and were the first subjects of early cyclostratigraphic analyses (Schwarzacher 1947, 1954; Fischer 1964): However, despite the long history of study, the origin of these carbonate cycles is still widely debated. The peritidal-subtidal Lofer cycles (Fischer 1964) were variously attributed to either allocyclic (Sander 1936; Schwarzacher 1954, 1993, 2005; Fischer 1964, 1975, 1991; Haas 1982, 1991, 1994; Schwarzacher and Haas 1986; Balog et al. 1997; Cozzi et al. 2005; Hinnov and Cozzi 2020) or autocyclic (Zankl 1967; Goldhammer et al. 1990; Satterley and Brander 1995; Satterley 1996; Enos and Samankassou 1998, 2021; Eberli 2013; Pollit et al. 2015; Samankassou and Enos 2019) processes. Although major advances have been made in the methodology of cyclostratigraphic analysis recently, the application of newly developed tools to the problem of Triassic carbonate cycles has remained limited (Hinnov and Cozzi 2020).\u003c/p\u003e\n\u003cp\u003eDuring the Late Triassic kilometer-thick cyclic carbonate successions (Main Dolomite and Dachstein Limestone Formations) were deposited on the vast Dachstein platform system, located on the northwestern passive margin of the Neotethys Ocean. Meter-scale peritidal-subtidal cycles formed in the internal belt of these platforms were described and termed as Lofer cycles (Fischer 1964). Remnants of these platforms are exposed extensively in the Northern Calcareous Alps (e.g. Sander 1936; Fischer 1964), the Southern Alps (e.g. Bossellini 1967; Boselini and Hardie 1988), the Central and Inner Western Carpathians (e.g. Michalik 1980, 1993), the Transdanubian Range (e.g. Haas 1994, 2004), the Dinarides (e.g. Dimitrijevic and Dimitrijevic 1982, 1991), and the Hellenides (Pomoni-Papaioannou et al. 1986; Pomoni-Papaioannou 2008) and offer an excellent opportunity for a comparative study of the cyclic sequences.\u003c/p\u003e\n\u003cp\u003eHere we present a detailed cyclostratigraphic analysis that employs the recently developed methodologies on the core Po-89 from the Bakony Mts. (Transdanubian Range, Hungary). The nearly complete lack of tectonic disturbances, the excellent recovery and preservation of the core, and the availability of previously recorded high-resolution datasets makes this core an exceptional candidate for a time-series analysis to tackle the long-standing issues about the Lofer cyclicity.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eVarious macroscopically observed properties of the logged core section (lithology, colour and greyscale indices, and Lofer cycle member attribution) at a resolution of 10 cm are used to investigate the possible Milankovitch scale orbital forcing in the succession. We evaluate if orbital forcing also drove the detected variability of cycle completeness. Finally, we develop a depositional model that may explain the cyclic depositional processes and compare our results to all other available cyclostratigraphic data to assess the similarities and differences in the cyclic nature of the Dachstein Limestone and analogous formations.\u003c/p\u003e\n\u003ch1\u003eGeological setting\u003c/h1\u003e\n\u003cp\u003eThe core Po-89 was drilled in 1979 near the village of Porva in the northern Bakony Mts. (Transdanubian Range, Hungary) (Fig. 1). The basal 33 m of the 408 m thick core section represents the uppermost part of the Fenyőfő Member, whereas the next 375 m belongs to the lower part of the overlying Dachstein Limestone Formation (Haas 1982). The Fenyőfő Member is a transitional unit between the typical Main Dolomite (\u003cem\u003eFődolomit\u003c/em\u003e, \u003cem\u003eHauptdolomit\u003c/em\u003e, or \u003cem\u003eDolomia Principale\u003c/em\u003e in the Hungarian, German, and Italian literature, respectively) and Dachstein Limestone. Here, the subtidal C members of the Lofer cycles are not entirely dolomitised and the supratidal A members are better developed than in the Main Dolomite (Haas 2004; Haas et al. 2015). The entire core section is Norian in age based on its Megalodontaceae fauna and foraminifera assemblages (Haas 1982, 1995b) and is free of any observable tectonic disturbance (Haas 1982).\u003c/p\u003e\n\u003cp\u003eThe studied core section represents a part of the Upper Triassic platform carbonate succession of the Transdanubian Range Unit which was a segment of the vast Dachstein carbonate platform system developed on the passive margin of the Neotethys Ocean (Fig. 1) (Balla 1982; Haas 1987, 2004; Haas et al. 1990). In the Transdanubian Range the thickness of the Upper Carnian to Middle Norian Lofer cyclic Main Dolomite is ~800\u0026ndash;1200 m, that of the transitional Fenyőfő Member is ~100\u0026ndash;400 m, whereas the Upper Norian to Rhaetian Dachstein Limestone Formation is ~600\u0026ndash;900 m thick (Haas 2004).\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eIn the Late Carnian the filling up of previously formed extensional basins led to a remarkably levelled topography and gave rise to the development of vast carbonate ramps/platforms. The Main Dolomite was deposited during the latest Carnian to mid-Norian under semi-arid climatic conditions, whereas increasing humidity during the Late Norian led to a gradual cessation of dolomitization (Balog et al. 1997;\u0026nbsp;Haas 2004; Haas et al. 2015). The deposition of this carbonate sequence was terminated at the end of the Rhaetian, possibly in relation with the end-Triassic events (P\u0026aacute;lfy et al. 2021). Dismemberment and subsequent drowning of most parts of the platform occurred near the Triassic-Jurassic boundary (Haas 1995a, b).\u003c/p\u003e\n\u003cp\u003eDuring the Alpine orogeny the entire Transdanubian Range Unit was incorporated into the Alpine nappe system as part of the ALCAPA Megaunit but it remained unmetamorphosed and largely intact (Balla 1982; Haas 1987, 2004; Haas et al. 1990). Thus, the ~2 km thick Lofer cyclic carbonate sequence can be studied in this area across its entire thickness with little or no distortion.\u003c/p\u003e"},{"header":"Methods","content":"\u003ch2\u003eCreation of the time-series\u003c/h2\u003e\n\u003cp\u003eThe original core log was digitized (Supplementary Material S1) and four different time-series (Lofer cycle member attribution, colour, greyscale, and lithology) were generated using uniform 10 cm sample spacing (Fig. 2). Firstly, numbers were assigned to the standard facies types, i.e. members of the Lofer cycles (Fischer 1964), as follows: member A and A\u0026rsquo; was marked with 1, member B and B\u0026rsquo; was marked with 2, and member C was marked with 3. Secondly, the colour of the rock was also converted to numbers, keeping the order in the original dataset as follows: 1 \u0026ndash; white, 2 \u0026ndash; yellow, 3 \u0026ndash; brown, 4 \u0026ndash; red, 5 \u0026ndash; green, 6 \u0026ndash; grey, 7 \u0026ndash; black. The original core description distinguished light, medium, and dark shades of the colours, except for the white and the black. This was indicated in the derived time-series as X.1 for a lighter shade, X.2 for a medium shade, and X.3 for a dark shade of colour X, where X is the number assigned to the base colour. Where two or more colours were indicated, we assigned their average value. Thirdly, as a more rigorous numeric approach, we assigned a greyscale value for all the colours and their different shades and used these values to create a greyscale time-series (Fig. S1). For a comparison of their performance, we calculated the correlation coefficients of the greyscale and colour time-series with the Lofer cyclicity and found that the greyscale record yields nearly four times higher correlation coefficients than the colours, thus more faithfully track the facies changes within Lofer cyclic series. The fourth time-series was created on the basis of lithology. The numeric values assigned to the different lithologies are summarized in Table 1. Where two or more types of lithology were indicated in the original log, their average value was used. All the generated time-series are provided in the Supplementary Material S2.\u003c/p\u003e\n\u003cp\u003e\u003cimg 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\"\u003e\u003c/p\u003e\n\u003ch2\u003eTime-series analysis\u003c/h2\u003e\n\u003cp\u003eThe cyclostratigraphic analyses were carried out using the \u003cem\u003eAcycle\u003c/em\u003e software (v2.4) (Li et al. 2019). The data preparation for each time-series that yielded the best results and the detailed settings of some of the applied methods are provided and discussed in the Chapter 1.2 of the Supplementary Material S3. Power spectra were generated using zero-padding (Bloomfield 1976), F-test, and the Multi-taper Method (MTM) (Thomson 1982; Mann and Lees 1996). The confidence levels for the power spectra were generated using the robust autoregressive model (robust AR(1)) (Mann and Lees 1996). The evolutionary spectra were generated using the Fast Fourier transform (LAH) method (Kodama and Hinnov 2015). To match the detected cycles with the Milankovitch cycles, the ratio method was used, which compares the ratio of the periods of the detected cycles to the ratio of the known period of the Milankovitch cycles. In addition, the quantitatively more robust COCO, eCOCO (Li et al. 2019), and TimeOpt, as well as eTimeOpt (Meyers 2015) methods were also applied to all of the time-series. For filtering, a Gaussian bandpass filter was used (Kodama and Hinnov 2015) and Coherence and phase analysis was also carried out to decipher the relationship between the different time-series. Wavelet analysis (Torrence and Compo 1998) was also performed on the Lofer cyclicity, colour and greyscale index time-series using the Acycle (v2.2) software.\u003c/p\u003e"},{"header":"Results","content":"\u003ch2\u003eIdentification of cycles and their linking to Milankovitch cycles\u003c/h2\u003e\n\u003cp\u003eThe cyclostratigraphic analysis reveals several spectral peaks (Table 2). The same cycles are found in all the analysed time-series (Fig. 3). However, the signal of some of the shortest cycles (with periods of less than 2 m) is affected by more noise, making their interpretation more difficult. Using the lithology time-series, the signal of the smaller cycles is weaker due to the inherently smaller variability. The clearest and most pronounced signals are detected for the cycles with periods of 32, 20, 13, 5.5, 4.5 and 3.6 m. Of these, the 13 and 3.6 m cycles are exceptionally robust in all the time-series. The largest cycle with a period of 66.6 m also displays a robust spectral peak but its frequency has a wider interval that causes its spectral power to be distributed, therefore it appears weaker.\u003c/p\u003e\u003ctable border=\"1\" cellspacing=\"0\" cellpadding=\"0\"\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e\u003cstrong\u003eFrequency (cycle/m)\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e\u003cstrong\u003ePeriod (m)\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e\u003cstrong\u003ePeriods of sedimentary cycles (kyr)\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e\u003cstrong\u003eThe identified orbitally-forced cycles and their period\u0026nbsp;\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.015\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e66.6\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e404\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eLong eccentricity (405 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.031\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e32.26\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e195.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e~200 kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.05\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e20\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e121.2\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eShort eccentricity (125 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.077\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e13\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e78.7\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eShort eccentricity (95 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.141\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e7.1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e42.9\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eObliquity (42.7 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.182\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e5.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e33.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eObliquity (34.2 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.223\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e4.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e27.2\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eObliquity (26.1 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.26\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e3.85\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e23.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eObliquity (25.3 kyr) and/or precession (21.2 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.28\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e3.6\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e21.65\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003ePrecession (21.2 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.3465\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e2.9\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e17.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003ePrecession (17.5 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.45\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e2.22\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e13.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eSemi/hemi-precession (~9\u0026ndash;13 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.635\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e1.575\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e9.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eSemi/hemi-precession (~9\u0026ndash;13 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.7\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e1.43\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e8.7\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eSemi/hemi-precession (~9\u0026ndash;13 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.78\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e1.28\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e7.77\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHeinrich events (~7\u0026ndash;8 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e0.855\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e1.17\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e7.1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHeinrich events (~7\u0026ndash;8 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e6\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e?\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e1.08\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.926\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e5.6\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHeinrich events or harmonics of precession (~4\u0026ndash;5 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e1.17\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.85\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e5.2\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHeinrich events or harmonics of precession (~4\u0026ndash;5 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e1.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.714\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e4.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHeinrich events or harmonics of precession (~4\u0026ndash;5 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e1.77\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.565\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e3.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHeinrich events or harmonics of precession (~4\u0026ndash;5 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e2.05\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.49\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e2.95\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e?\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e2.22\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.45\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e2.73\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e?\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e2.535\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e2.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHallstatt or Bray solar activity cycles (~2.3 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e2.94\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.34\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e2.06\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eHallstatt or Bray solar activity cycles (~2.3 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e3.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e1.84\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e?\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e3.53\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.283\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e1.72\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003e?\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e3.8\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.263\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e1.6\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eDansgaard\u0026ndash;Oeschger cycles (~1.3\u0026ndash;1.6 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e4.1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.244\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e1.48\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eDansgaard\u0026ndash;Oeschger cycles (~1.3\u0026ndash;1.6 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"12.417218543046358%\" valign=\"top\"\u003e\n \u003cp\u003e4.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.609271523178808%\" valign=\"top\"\u003e\n \u003cp\u003e0.23\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"32.11920529801324%\" valign=\"top\"\u003e\n \u003cp\u003e1.41\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"46.854304635761586%\" valign=\"top\"\u003e\n \u003cp\u003eDansgaard\u0026ndash;Oeschger cycles (~1.3\u0026ndash;1.6 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n\u003c/table\u003e\n\u003cp\u003e\u003cstrong\u003eTable 2\u003c/strong\u003e Matching of the detected periodicities with the Milankovitch cycles at a sedimentary rate of 16.5 cm/kyr. The cycles within the sub-Milankovitch range are shown below the double line. The periods of the Milankovitch cycles are based on the La2004 model for 218 Ma (Laskar et al. 2004). See text for a discussion of the periods of the sub-Milankovitch cycles\u003c/p\u003e\n\u003cp\u003eTo link the observed cycles with the Milankovitch cycles, determination of the sedimentary rate is of paramount importance. The COCO and eCOCO method yield a stable sedimentary rate of either ~3 or ~13\u0026ndash;17 cm/kyr. However, the TimeOpt and eTimeOpt methods only support a stable sedimentary rate of c. 15 cm/kyr (Fig. 4). The lower, ~3 cm/kyr sedimentary rate is indeed unlikely, because in that case the ~2\u0026ndash;3 m thick Lofer cycles in the Transdanubian Range (Haas 1982, 1994, 2004; Balog et al. 1997) would represent the ~100 kyr short eccentricity cycle, implying a more than 80 Myr duration for the deposition of the ~2 km thick Lofer cyclic carbonate sequence. However, independent stratigraphic constraints suggest that this succession is confined to only a part of the Late Triassic. A sedimentary rate around 15 cm/kyr would closely match the Lofer cycles with the precession cycles as suggested by earlier studies (Sander 1936; Schwarzacher 1954, 1993, 2005; Fischer 1964; Garrison and Fischer 1969; Schwarzacher and Haas 1986; Haas 1994; Balog et al. 1997; Cozzi et al. 2005; Hinnov and Cozzi 2020). Thus, having broadly established the most likely sedimentary rate as c. 15 cm/kyr, we used the ratio method to determine the sedimentary rate that would provide the best match between the ratios of the periods of the identified cycles and the Milankovitch cycles. The best result falls in the higher part of the range of possible sedimentary rates, at ~16.5 cm/kyr.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eMatching of the here identified cycles with the orbitally forced (i.e. Milankovitch and sub-Milankovitch) cycles is presented in Table 2. The match between the calculated periods of the identified cycles and the expected periods of the Milankovitch cycles (Laskar et al. 2004, 2011; Hinnov and Hilgen 2012) is exceptionally good for the Late Triassic, only the peculiar ~200 kyr cycle needs further consideration. Previously, any detected cycle in the ~200\u0026ndash;250 kyr range was not regarded as a true orbital cycle. However, several recent studies suggest that indeed it may represent a real orbital cycle (e.g. Friedrich et al. 2008; Liebrand et al. 2016; Hilgen et al. 2015). Hilgen et al. (2020) suggested that this cycle either arises from the non-linear response to the astronomical forcing or, more likely, from the alternation of strong and weak ~100 kyr minima in short eccentricity. Alternatively, Huang et al. (2021) argued that a ~173 kyr cycle may result from obliquity forcing. Thus, although a ~200 kyr cycle may reflect orbital forcing in the sedimentary record, its origin remains debated. As the here studied Lofer cycles were formed at low paleolatitude, an eccentricity-related origin is more plausible.\u003c/p\u003e\n\u003cp\u003eAt the sub-Milankovitch scale, i.e. for periods less than ~17\u0026ndash;20 kyr, the matching is more difficult in the lack of established target cycle periods. The most prominent sub-Milankovitch cycles found here are the 13.5, 3.4, 2.4, and 1.48 kyr cycles. In addition, noisier but still significant cycles occur with periods of 5 and 7 kyr. A detailed treatment of their possible origin is given in the relevant subsection of the Discussion.\u003c/p\u003e\n\u003ch2\u003eDuration of deposition recorded in the core Po-89\u003c/h2\u003e\n\u003cp\u003eTo determine the time of deposition recorded in the studied section of the core Po-89, the 405 kyr long eccentricity, the 95 kyr short eccentricity, the 34 kyr obliquity and the 21 kyr precession signals are filtered from all the time-series, then tuned to the respective cycles. The resulting duration consistently falls in the range of 2.42\u0026ndash;2.58 Myr, with an average of 2.487 Myr. Thus, the studied core Po-89 represents an approximately 2.5 Myr interval of carbonate platform deposition within the Norian.\u003c/p\u003e\n\u003ch2\u003eOther observations from the cyclostratigraphic analysis\u0026nbsp;\u003c/h2\u003e\n\u003cp\u003eThe evolutionary spectra of the studied time-series consistently reveal three intervals with lower levels of spectral power (Fig. 5). These are as follows: from -94.4 m (top of the core) to -140 m, from -240 m to -330 m, and from -480 m to -502.1 m (bottom of the core). The first two likely result from the overall smaller variance in the time-series within these intervals, whereas the third interval entirely represents the partially dolomitized Fenyőfő Member.\u003c/p\u003e\n\u003cp\u003eAccording to the wavelet analyses and the evolutionary spectra, along the more prominent erosional surfaces usually only the signal of the cycles with periods of less than 2 m is distorted (Fig. 6). However, there are two erosional surfaces (at -204 and -290 m) where the signal of the cycles with periods up to 4 m period is also distorted. Nonetheless, these observations suggest that the succession is most likely complete even at the level of the Lofer cycles (i.e. at the precession scale) and definitely undisturbed at the obliquity and eccentricity scale.\u003c/p\u003e\n\u003cp\u003eCoherence and phase analyses reveal that the lighter colours and greyscale values consistently belong to the members C in the Lofer cycles, whereas the darker colours and greyscale values consistently belong to the members A. Members C also correspond to lower values of the lithological index, i.e. limestone or dolomite, whereas members A correspond to higher lithological index values, i.e. more argillaceous lithologies. These findings are in good agreement with the macroscopic observations.\u003c/p\u003e"},{"header":"Discussion","content":"\u003ch2\u003eCyclic depositional model\u003c/h2\u003e\n\u003cp\u003eThe Upper Triassic Lofer cyclothems in the Northern Calcareous Alps and their elementary Lofer cycles were originally defined and described as unconformity-bounded, deepening-upward (i.e. transgressive) sedimentary cycles that are made up of three characteristic lithofacies types, referred to as Lofer cycle members A, B, and C (Fischer 1964). Member A consists of red or green marl or claystone that commonly contains pebble-sized clasts of penecontemporaneous limestone. Member B is characterized by stromatolites and/or fenestral laminites (loferites) with common occurrence of desiccation features. Member C is made up of carbonates with wackestone or packstone texture that contain shallow marine fossils, including locally abundant megalodontids and benthic foraminifera. Originally, members A and B were interpreted as tidal flat deposits that were formed in the supratidal and intertidal zones, respectively, whereas member C is characteristic to the subtidal zone (Fischer 1964). Subsequently, however, it was recognised that the ideal elementary Lofer cycle shows a symmetrical A-B-C-B\u0026rsquo;(-A\u0026rsquo;) pattern (Haas 1982). The regressive member B\u0026rsquo; is similar to the transgressive member B but it is commonly mud-cracked, leached, and, in some cases, more intensely dolomitized (Haas 1982, 1994).\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eThe typical Lofer cyclic successions were deposited on the inner (i.e. more coastal) part of the platform, characterized with a very gently sloping (~1\u0026deg;) ramp-like topography. The adjacent outer platform had a slightly steeper slope, stabilized by primarily microbial, and subordinately metazoan mounds (\u0026quot;microbial reefs\u0026quot;) and oncoidal mounds accumulated by vigorous currents. Thus, although typical Lofer cycles did not form on the outer part of the platform system, nevertheless the outer platform could also influence the deposition on the inner platform via the so-called basket effect (Haas 1994, 2004).\u003c/p\u003e\n\u003cp\u003eDuring a lowstand, large areas of the inner platform become subaerially exposed and are subjected to karstification and pedogenic processes, while most of the outer platform remains submerged. At the onset of the transgression, as the sea level starts to rise and reaches the inner platform, first the terrestrial sediments and the erosional products are reworked and redeposited (member A). Subsequently, if the sea level rise is slow, a microbial mat-covered tidal flat environment is established (member B). In this scenario, there is no basket effect and the platform behaves as a ramp-like platform, leading to the development of an ideal Lofer cycle. On the contrary, when the basket effect applies and/or the sea level rise is too rapid, most of the inner platform immediately transitions into the subtidal zone where member C is deposited. This model may explain the occasionally missing A and/or B members. After reaching the maximum flooding, during the late highstand, normal regression occurs and, with the reduction of the available accommodation space, the inner platform transitions into a tidal flat covered by microbial mats again (member B\u0026rsquo;). If this process is too fast, member B\u0026rsquo; may be missing entirely. In both cases, however, member B\u0026rsquo; could also be removed by erosion, when forced regression takes place and the inner platform becomes subaerially exposed again at the end of the sequence. This leads to the development of a disconformity, occasionally with the presence of member A\u0026rsquo; (Haas 1982, 1994, 2004).\u003c/p\u003e\n\u003cp\u003eThese cyclic sea level fluctuations are hypothesized to be of a few metres to 15 m in amplitude (Fischer 1964; Haas 1994; Balog et al. 1997) and commonly associated with orbitally forced eustatic sea-level variations (Sander 1936; Schwarzacher 1954, 1993, 2005; Fischer 1964, 1975, 1991; Haas 1982, 1991, 1994; Schwarzacher and Haas 1986; Balog et al. 1997; Cozzi et al. 2005; Hinnov and Cozzi 2020). From the Late Carnian to the Rhaetian, the Dachstein platform was not affected by any significant tectonic deformation and only a prolonged, slow and gradually accelerating subsidence is assumed (Haas 1994).\u003c/p\u003e\n\u003cp\u003ePreviously, the thermal expansion of sea water was hypothesized as the most likely driving force of orbitally-driven sea-level fluctuations during greenhouse climate states, supported by modeling that showed that this process can generate sea level variations up to 2 m (Schulz and Sch\u0026auml;fer-Neth 1997). More recently, however, aquifer- and limno-eustasy is increasingly accepted as a more potent driving force as several studies suggested that the water-bearing potential of groundwater aquifers and lakes in greenhouse climate state is about equal to that of polar ice caps during icehouse intervals (Southam and Hay 1981; Hay and Leslie 1990; Wagreich et al. 2014; Peters and Husson 2015; Wendler et al. 2016).\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eAquifer- and limno-eustasy continuously redistributes water between the oceans and continents. During the maximum of seasonality, the hydrological cycle strengthens, and water is delivered from the oceans to the continents via precipitation. The continental surface and subsurface reservoirs such as lakes and groundwater aquifers recharge, the water levels of the lakes rise while, at the same time, the global sea level falls. During the minimum of seasonality, the hydrological cycle weakens, and the continental reservoirs discharge via fluvial runoff. This would lead to a lowering of water level in lakes and concomitant sea level rise (Wagreich et al. 2014; Li et al. 2016; Wendler et al. 2016; Li et al. 2018). Several recent studies document the antiphase relationship between variations of sea level and lake water levels linked by orbital forcing in the Mesozoic (e.g. Wagreich et al. 2014; Li et al. 2018). One such study is especially relevant as it demonstrated the relationship between sea level variations observed in Lofer cycles in the Southern Alps and lake level variations in the Newark Basin (Hinnov and Cozzi 2020). In addition, ˝megamonsoon˝-driven aquifer- and limno-eustasy is proposed from the partly coeval intraplatform Csőv\u0026aacute;r basin that was located on the outer part of the Dachstein platform system in the Transdanubian Range (Vallner et al. 2023).\u003c/p\u003e\n\u003cp\u003eOur analysis of the core Po-89 reveals that the thickest members C were deposited consistently during long eccentricity minima, when the climate was more balanced, and seasonality could reach its absolute minima. This finding is in agreement with the concept of aquifer- and limno-eustasy that predicts that the long eccentricity minima are associated with generally higher sea level and increased accommodation space, promoting the deposition of thick members C. In the opposite phase, during the long eccentricity maxima, although conditions may favour the formation of members A, they do not become thicker or more common in the record. As member A is pedogenic and redeposited in origin and prone to erosion, this observation does not contradict the model of aquifer- and limno-eustatic control.\u003c/p\u003e\n\u003ch2\u003eOrbital forcing on the completeness of the Lofer cycles\u003c/h2\u003e\n\u003cp\u003eThe common occurrence of symmetrical A-B-C-B\u0026rsquo;(-A\u0026rsquo;) Lofer cycles was first described from the core Po-89, but incomplete cycles with depositionally missing members and/or truncated cycles that were affected by a higher degree of subaerial erosion were also encountered (Haas 1982). This observation raises the possibility of orbital forcing of the different completeness of the cycles preserved in the sedimentary record. To test this hypothesis in general, and to assess if the dominant cycle types and average cycle completeness differs at long eccentricity minima and maxima, here we apply time-series analysis on the cycle completeness. First, a completeness index was developed to categorize each cycle, based on the subdivision described by Haas (1998) (Table 3). Then, time-series analysis was carried out using the same data preparation steps and settings for the power and evolutionary spectra generation as for the analyses of other time-series.\u003c/p\u003e\n\u003cdiv align=\"center\"\u003e\n \u003ctable border=\"1\" cellspacing=\"0\" cellpadding=\"0\"\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd\u003e\n \u003cp\u003e\u003cstrong\u003eIndex value\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003e\u003cstrong\u003eDescription\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003e\u003cstrong\u003eCycle types\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd\u003e\n \u003cp\u003e1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003eIdeal, symmetric, complete cycles\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003edABCB\u0026apos;A\u0026apos;d; dABCB\u0026apos;d\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd\u003e\n \u003cp\u003e2\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003eIncomplete cycles with depositionally missing members\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003edBA\u0026apos;d; dCB\u0026apos;d; dCA\u0026apos;d; dBCB\u0026apos;d; dACB\u0026apos;d; dABCA\u0026apos;d\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd\u003e\n \u003cp\u003e3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003eTruncated cycles with higher degree of subaerial erosion at their top\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003edABCd\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd\u003e\n \u003cp\u003e4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003eIncomplete and truncated cycles\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd\u003e\n \u003cp\u003edACd; dCd\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e\n\u003cp\u003e\u003cstrong\u003eTable 3\u003c/strong\u003e\u003cem\u003e\u0026nbsp;\u003c/em\u003eCompleteness index used to test the possible orbital forcing of the different completeness of the Lofer cycles. d \u0026ndash; disconformity, i.e. erosion between the different cycle members\u003c/p\u003e\n\u003cp\u003eWe found that during the long eccentricity maxima the average of the completeness indices of the cycles was consistently lower than during long eccentricity minima, with only one exception (at a long eccentricity minimum between -147 and -177 m). The average value of all long eccentricity maxima is 1.5, in stark contrast to the average of 2.7 of all long eccentricity minima. The complete, symmetrical cycles are more common during the maxima, whereas the minima are dominated by the incomplete and truncated cycle type. The purely incomplete and purely truncated Lofer cycle types do not dominate any orbital cycle segments; they are nearly evenly distributed along the long eccentricity curve (Fig. 7).\u003c/p\u003e\n\u003cp\u003eThe results of the time-series analysis of the completeness index are noisier but they are in agreement with the other time-series analyses performed. However, due to the lower resolution of the completeness index, the majority of the sub-Milankovitch cycles are not detectable by this method (Fig. 8).\u003c/p\u003e\n\u003cp\u003eOur results imply that the different completeness of the Lofer cycles is also driven by Milankovitch-scale orbital forcing, possibly through the changing pace of sea level variations controlled by the available water mass in the oceans. As a consequence of aquifer- and limno-eustasy, long eccentricity maxima are associated with less available water mass in the oceans and thus generally lower sea level. As a result, slower changes of sea level are expected that, together with the effect of lower sea level, would lead to a complete development of each facies types within the Lofer cycle. On the contrary, during long eccentricity minima, when the available water mass is greater, the sea level is generally higher, and subsequently the sea level changes are faster, the inner platform would remain mostly in the subtidal zone and enter the intertidal zone for only a short period of time that is insufficient for the members B and B\u0026rsquo; to develop properly. In this case, commonly only a disconformity surface is formed that marks a brief subaerial exposure. These conditions also explain the detected higher thickness of members C during long eccentricity minima.\u003c/p\u003e\n\u003cp\u003eThe time-series analysis of the completeness index revealed another peculiar phenomenon. A comparison of the evolutionary spectra (Fig. S2) allows the identification of three segments (from -94.4 m to -140 m, -240 m to -330 m, and -480 m to 502.1 m, respectively) where the original time-series yields lower levels of spectral power, as opposed to the higher levels of spectral power in the completeness index time-series. On the contrary, all other segments with higher levels of spectral power in the original time-series are found to exhibit less spectral power in the completeness index time-series. A plausible explanation of this antiphase relationship calls for oppositely changing variance in the original time-series and the completeness index time-series. Thus, when the variability among the different cycle types is higher, i.e. more types are alternating more frequently, then the variability within the Lofer facies types is lower. Then, fewer facies types and a more limited range of lithology, colour, and greyscale values are alternating, and do so with a lower frequency. The changing variability among these segments exhibited by the completeness index time-series is also apparent in Fig. 7.\u003c/p\u003e\n\u003cp\u003eWe suggest that this pattern stems from the inherent properties of the genesis and preservation of Lofer cycles. The maximum variance in the Lofer facies types, as also reflected in the broadest range of lithology, colour, and greyscale indices, occurs when most of the Lofer cycles are complete and there is only limited deviation from the ideal type, i.e. minimal variance among the cycle types. It follows that changes in variance may also be paced by the orbital cycles as the dominance of the complete cycle type is proved to be controlled by the long eccentricity cycle. Since there are only three complete segments of higher and lower variability within the core, time-series analysis cannot offer a rigorous test for this hypothesis, yet the similar thicknesses of these segments may still hint at regular cyclicity. The thickness of these segments is 100, 90, and 150 m, respectively, which may form parts of larger cycles with periods of 190\u0026ndash;240 metres. Notably, Schwarzacher (2005) also reported the presence of 190\u0026ndash;240 m thick cycles from the bundles of Lofer cycles in the Leoganger Steinberge section in the Northern Calcareous Alps. A conversion of the thickness of this, as yet hypothetical cycle to time domain, using a sedimentary rate of 16.5 cm/kyr as determined in this study, yields a period of 1.15\u0026ndash;1.45 Myr. Remarkably, there is a striking coincidence of this period with that of the ~1.2\u0026ndash;1.3 Myr grand orbital cycle (Lourens and Hilgen 1997; Li et al. 2018; Boulila 2019), pointing to another level in the hierarchy of orbital control exhibited in Lofer cyclic successions.\u003c/p\u003e\n\u003ch2\u003eSub-Milankovitch cycles\u003c/h2\u003e\n\u003cp\u003eAnother notable outcome of our cyclostratigraphic analyses is the identification of 19 cycles in the sub-Milankovitch band, i.e. with periods of less than ~17\u0026ndash;20 kyr (Table 2). The most prominent among them are the cycles of 13.5, 7, 5, 3.4, 2.4, and 1.48 kyr. Currently there are no established target cycles for the Mesozoic in this scale, which makes their matching to known cycles challenging. However, several recently published cyclostratigraphic studies report sub-Milankovitch cycles from the Mesozoic, therefore a comparison with their results may provide further insights, despite the lack of agreement on the driving forces of these cycles.\u003c/p\u003e\n\u003cp\u003eThe most characteristic sub-Milankovitch cycles identified in other studies for the Mesozoic are the cycles of ~9\u0026ndash;13, ~7\u0026ndash;8, ~4\u0026ndash;5, and ~1.5\u0026ndash;2 kyr (Rodr\u0026iacute;guez-Tovar and Pardo-Ig\u0026uacute;zquiza 2003; Z\u0026uuml;hlke et al. 2003; Kent et al. 2004; Friedrich et al. 2005; Vollmer et al. 2008; Boulila et al. 2010; Wu et al. 2012; De Winter et al. 2014; Chu et al. 2020; Boulila et al. 2022; Hasegawa et al. 2022; Ma et al. 2022; Zhang et al. 2023a). Several recent studies propose a link of the ~9\u0026ndash;13 kyr cycle with the so-called hemi- or semi-precession cycle (Rodr\u0026iacute;guez-Tovar and Pardo-Ig\u0026uacute;zquiza 2003; Vollmer et al. 2008; Wu et al. 2012; Chu et al. 2020; Zhang et al. 2023a). Theoretically, a cycle with half the period of the precession may arise from the insolation maxima due to the biannual passage of the Sun across the intertropical zone (Berger and Loutre 1997; Berger et al. 2006). In the context of the present study, however, an alternative explanation, that these cycles may arise from the occurrence of incomplete or truncated Lofer cycles, cannot be ruled out. The ~7\u0026ndash;8 kyr cycle was linked to the Heinrich events (e.g. De Winter et al. 2014), even though the Heinrich events were originally described from the last glacial period and are thought to correspond to ice sheet melting (Heinrich 1988). However, recent studies suggest that this cycle may originate in the tropical areas, as the nonlinear response to precession-induced insolation variations and subsequent changes in El Ni\u0026ntilde;o frequency (e.g. Turner 2004; Ziegler 2009). The the ~4\u0026ndash;5 kyr cycles are also linked to either the Heinrich events (Hasegawa et al. 2022) or the harmonics of the precession (Chu et al. 2020), whereas the ~1.5\u0026ndash;2 kyr cycles are associated with either the 1.3\u0026ndash;1.6 kyr Dansgaard\u0026ndash;Oeschger (DO) cycles modulated by the precession cycle and its harmonics (Boulila et al. 2022; Hasegawa et al. 2022) or the ~1 kyr Eddy and ~2.3 kyr Hallstatt or Bray solar activity cycles (Hasegawa et al. 2022; Ma et al. 2022). The DO cycles were originally described from records of the last glacial period (Dansgaard et al. 1982) but recent studies also established the presence of a cycle with similar period in the Mesozoic (Boulila et al. 2022; Hasegawa et al. 2022; Ma et al. 2022). Moreover, the controversial Latemar couplets also appear associated with a ~1.7\u0026ndash;2.2 kyr cycle (Kent et al. 2004).\u003c/p\u003e\n\u003cp\u003eOur results provide additional support to the conclusions of the studies cited above, as we suggest that the 8.7\u0026ndash;13.5 kyr cycles likely represent the semi/hemi-precession cycles, the 7.1\u0026ndash;7.77 kyr cycles the Heinrich events, the 3.4\u0026ndash;5.6 kyr cycles also the Heinrich events or harmonics of the precession cycle, the 2.06\u0026ndash;2.4 kyr cycles the Hallstatt or Bray solar activity cycles, and the 1.4\u0026ndash;1.6 kyr cycles the DO cycles (Table 2). However, to explain the origin of the 1.72\u0026ndash;1.84, 2.73\u0026ndash;2.95, and 6 kyr cycles remains challenging. Tentatively we propose that the 1.72\u0026ndash;1.84 kyr and 2.73\u0026ndash;2.95 kyr cycles may be similar to the Latemar couplets with an as yet unknown driving force or, alternatively, may be related to either the DO cycles or solar activity cycles, whereas the 6 kyr cycle may represent another expression of the Heinrich events or harmonics of the precession.\u0026nbsp;\u003c/p\u003e\n\u003ch2\u003eComparison with other Lofer cyclic successions\u003c/h2\u003e\n\u003cp\u003eAs the allocyclic vs autocyclic nature of the Lofer cyclothems has long been debated, a regional comparison is warranted and may yield additional insights. From the Alps to the Hellenids, we comprehensively collected the available data on the thickness of the individual Lofer cycles, the thickness and proposed period of the other identified cycles, and sedimentary rates within the Lofer cyclic successions (Table 4). To validate the hypothesis of orbital forcing, a high degree of similarity in the cyclic pattern of geographically distant study areas is expected.\u0026nbsp;\u003c/p\u003e\n\u003ctable border=\"1\" cellspacing=\"0\" cellpadding=\"0\" width=\"970\"\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\"\u003e\n \u003cp\u003e\u003cstrong\u003eReference\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\"\u003e\n \u003cp\u003e\u003cstrong\u003eLocation of the studied section(s)\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\"\u003e\n \u003cp\u003e\u003cstrong\u003eThickness of an individual Lofer cycle\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\"\u003e\n \u003cp\u003e\u003cstrong\u003eIdentified cycles\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\"\u003e\n \u003cp\u003e\u003cstrong\u003eCalculated sedimentary rate\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\"\u003e\n \u003cp\u003e\u003cstrong\u003eMethod(s) used\u0026nbsp;\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eSchwarzacher (1954)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eLoferer Steinberge, Northern Calcareous Alps, Austria\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003eaverage 3.5 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e3.5 m (~20 kyr) \u0026amp; 15\u0026ndash;18 m (~100 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003esuggested by bundling pattern\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eFischer (1964)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eDachstein, Leoganger Steinberge, Steinernes Meer \u0026amp; Loferer Steinberge sections, Northern Calcareous Alps, Austria\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e5\u0026ndash;6 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e~20, 50 \u0026amp; 100 kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~11 cm/kyr*\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003ethickness divided by time \u0026amp; Fischer-plot\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eSchwarzacher and Haas (1986)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eLoferer Steinberge, Steinernes Meer \u0026amp; Dachstein sections, Northern Calcareous Alps, Austria and cores T-5, Po-89 \u0026amp; Ut-8, Transdanubian Range, Hungary\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003eaverage 3.5 m (Loferer Steinberge), 5.69 m (Steinernes Meer), 4.84 m (Dachstein), 2.21 m (T-5 core), 3.1 m (Po-89 core) \u0026amp; 4.29 m (Ut-8 core)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e2.5\u0026ndash;4 m (~20 kyr), 5\u0026ndash;7 m (~40\u0026ndash;45 kyr), 12\u0026ndash;15 m (~100 kyr), 20\u0026ndash;27 m (~150\u0026ndash;200 kyr) \u0026amp; 45 m (~300 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~13\u0026ndash;23 cm/kyr, most likely within 13.3\u0026ndash;16.5 cm/kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003ethickness divided by time, Fischer-plot \u0026amp; Walsh power spectra on Lofer ABC indices from the Loferer Steinberge and the Hungarian core sections\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eHaas (1982, 1994, 2004)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eTransdanubian Range\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e2\u0026ndash;5 m, average 3.1 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~15\u0026ndash;16 cm/kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003ethickness divided by time\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eBalog et al. (1997)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eCores Ut-8, Zt-62, E-5, T-5, Td-4 \u0026amp; Po-89, Transdanubian Range, Hungary\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e1\u0026ndash;5 m, average 3.1 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e2\u0026ndash;3 m (~20 kyr), 5\u0026ndash;7 m (~35\u0026ndash;45 kyr), 12\u0026ndash;14 m (~90\u0026ndash;100 kyr), 33 m, 40\u0026ndash;50 m (~400 kyr) \u0026amp; 99 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~10\u0026ndash;16 cm/kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003ethickness divided by time, Fischer-plot on cores Ut-8, Po-89, T-5, Zt-62 \u0026amp; Td-4 \u0026amp; Walsh and Fast Fourier Transform (FFT) power spectra on Lofer ABC indices from core Po-89\u0026nbsp;\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eCozzi et al. (2005)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eMonte Canin section, Julian Alps, Italy\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003eaverage 2.41 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e1.6\u0026ndash;3.5 m (~20 kyr), 13.7 m (~100 kyr) \u0026amp; 54 m (~400 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~8\u0026ndash;18 cm/kyr*\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003emultiple power spectra and evolutionary spectra on greyscale indices created from field photographs\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eSchwarzacher (2005)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eLoferer Steinberge, Leoganger Steinberge \u0026amp; Steinernes Meer sections, Northern Calcareous Alps, Austria\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e2\u0026ndash;3.5 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e2\u0026ndash;3.5 m (~20 kyr), 5\u0026ndash;7 m, 9\u0026ndash;13 m, 15\u0026ndash;27 m (~100 kyr), 60\u0026ndash;80 m (~400 kyr), 190\u0026ndash;240 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~15\u0026ndash;20 cm/kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003eLomb-Scargle analysis on greyscale indices created from field photographs from the Leoganger Steinberge\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eHaas and Pomoni-Papaioannou (2009)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eArgolis Peninsula, Hellenids, Greece\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e1\u0026ndash;5 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eTodaro et al. (2017)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eMonte Sparagio section, Sicily, Italy\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e0.8\u0026ndash;3 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\"\u003e\n \u003cp\u003e\u0026mdash;\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eHinnov and Cozzi (2020)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eMonte Canin section, Julian Alps, Italy\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003eaverage 2.41 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e2\u0026ndash;3.1 m (~17\u0026ndash;23 kyr), 4.46\u0026ndash;8.3 m (~30\u0026ndash;50 kyr), 17.3 m (~100 kyr) \u0026amp; 21.3\u0026ndash;39.5 m (~400 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~15\u0026ndash;17 cm/kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003eMTM power spectra, FFT evolutionary spectra, and tune and release method on the data from Cozzi et al. (2005)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd width=\"9.175257731958762%\" valign=\"top\"\u003e\n \u003cp\u003eThis study\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.927835051546392%\" valign=\"top\"\u003e\n \u003cp\u003eCore Po-89, Transdanubian Range, Hungary\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"16.5979381443299%\" valign=\"top\"\u003e\n \u003cp\u003eaverage 3.1 m\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"20.61855670103093%\" valign=\"top\"\u003e\n \u003cp\u003e2.9\u0026ndash;3.6 m (~17.5\u0026ndash;21.6 kyr), 3.85\u0026ndash;7.1 m (~23.3\u0026ndash;42.9 kyr), 13\u0026ndash;20 m (~78.7\u0026ndash;121.2 kyr), 32.3 m (~200 kyr) \u0026amp; 66.6 m (~404 kyr)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"8.65979381443299%\" valign=\"top\"\u003e\n \u003cp\u003e~16.5 cm/kyr\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd width=\"24.02061855670103%\" valign=\"top\"\u003e\n \u003cp\u003eSee Chapter 3\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n\u003c/table\u003e\n\u003cp\u003e\u003cstrong\u003eTable 4\u003c/strong\u003e Summary of published cyclostratigraphic analyses of Lofer cyclic successions, with the estimated thickness of individual Lofer cycles, detected periods and their matching with orbital cycles, calculated sedimentary rates, and the method(s) used in each study. If the sedimentary rate was not given in the original study, it is calculated here (denoted by an asterisk) from the known and matched periods of the detected cycles\u003c/p\u003e\n\u003cp\u003eThe thickness of the Lofer cycles consistently falls between 1 and 6 m, with an average thickness of 2.5\u0026ndash;3.5 m, whereas the inferred sedimentary rate is also consistent between 10 and 20 cm/kyr. Most studies suggest the precession cycle as the driving force for the basic cycle, in accordance with the earlier assumption (Sander 1936; Fischer 1991; Schwarzacher 1993), except one study that suggested obliquity forcing, although based on limited data only (Fischer 1964). Each study that was based on detailed cyclostratigraphic analysis successfully identified the short and long eccentricity cycles with periods of ~12\u0026ndash;17 m and ~50\u0026ndash;70 m, respectively, whereas five out of six studies also found cycles in the frequency band of obliquity (with periods between ~4\u0026ndash;7 m) and a cycle with a ~30 m period. The similarity between the periods is remarkable. All the studies reported a robust short eccentricity signal exhibited in the bundling pattern of the individual Lofer cycles, whereas the long eccentricity signal appears weaker, more fragmented, distorted, or ambiguous. The latter finding is consistent with the observation of less clear and obvious 20:1 bundling pattern of the Lofer cycles (Haas 1982; Haas and Schwarzacher 1986; Goldhammer et al. 1990; Balog et al. 1997).\u003c/p\u003e\n\u003cp\u003eThese similarities among sections in the Northern Calcareous Alps, the Transdanubian Range, the Southern Alps, Sicily, and the Hellenids imply that regular cyclicity was not an isolated phenomenon but rather a prevalent depositional feature in the entire Dachstein platform system (Fig. 9). Consequently, Milankovitch-scale orbitally forced eustatic sea level variations remain the only plausible cause for the near-uniform cyclicity that affected such a broad paleogeographic area for an extended period of time. Although the local effect of autocyclic processes on the sedimentation cannot be ruled out entirely, their role was much more limited.\u003c/p\u003e\n\u003cp\u003eMost of the studies that question the orbital forcing present arguments that the Lofer cycles have lateral thickness variations, occasionally they pinch out, and many cycles are not complete (Satterley and Brander 1995; Enos and Samankassou 1998, 2021; Samankassou and Enos 2019). In addition, questions were raised about the consistency of the stacking pattern and the viability of a driving force in a greenhouse world (Goldhammer et al. 1990; Satterley and Brander 1995; Satterley 1996).\u003c/p\u003e\n\u003cp\u003eTo fend off these criticisms, it was pointed out that lateral variability was observed only in the Steinerness Meer section but elsewhere, in other sections studied in the Northern Calcareous Alps, lateral variations are rather rare (Schwarzacher 2005). Concerns of the consistency of stacking pattern were based solely on visual observation or Fischer-plots, rather than on detailed cyclostratigraphical analysis (Schwarzacher 2005). Although the core Po-89 used in this study obviously does not afford an opportunity to examine lateral variations, it is eminently suitable to detect orbital forcing due to the exceptional preservation of the cycles. As demonstrated in Table 4, our results are coherent with the other, originally distant parts of the Dachstein platform system (Fig. 9). It is not conceivable that random processes would produce highly similar, hierarchical sedimentary cyclicity across a wide geographic area and through an interval of millions of years, such as the spatial and temporal extent of the Dachstein platform system. The credibility of our results obtained using up to date cyclostratigraphic tools is also supported by the demonstration of the reliability and sensitivity of this methodology (Sinnesael et al. 2019).\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eAn independent line of supporting arguments is provided by studies of the Upper Triassic to lowermost Jurassic carbonates deposited in the peri- and intraplatform basins of the Dachstein platform system. These deposits consist of calciturbidites that were sourced primarily from the adjacent platforms (Vallner et al. 2023). As Milankovitch cyclicity was identified in several of these deposits (Mesetti et al. 1989; Reijmer and Everaars 1991; Reijmer et al. 1993; Maurer et al. 2004; Vallner et al. 2023), it is highly likely that the deposition in the platforms and the adjacent basins were both paced by the same orbital cycles.\u003c/p\u003e\n\u003cp\u003eOur discussion of the results of this study is intended to help to settle the debate that has been going on for more than 70 years. The definitive evidence for orbital forcing of the sedimentation in the Late Triassic platforms validates the use of cyclostratigraphy and astrochronology as high-resolution stratigraphic tools for the Dachstein Limestone Formation and its analogues. In addition, comparison of the Upper Triassic cyclothems with the younger platform deposits that record orbitally forced cycles, as in the Arabian and the Adriatic Platforms, will further our understanding of the general patterns of cyclic sedimentation in the Mesozoic carbonate platform environments.\u003c/p\u003e"},{"header":"Conclusions","content":"\u003cp\u003e1) The detailed archive log of a more than 400 m thick record of the cyclic Norian Dachstein Limestone in the Po-89 core was suitable to produce a high-resolution time-series of Lofer facies type, colour, greyscale, and lithology at 10 cm sample spacing.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e2) Cyclostratigraphic analysis successfully revealed several spectral peaks that could be confidently matched with the Milankovitch cycles. Cycles with a period of 3.6 m are especially robust and represent the elementary Lofer cycles that correspond to orbital precession cycles with a period 21.65 kyr.\u003c/p\u003e\n\u003cp\u003e3) The sedimentary rate is determined as 16.5 cm/kyr, thus the studied section in the core Po-89 represents 2.5 Myr of carbonate platform evolution.\u003c/p\u003e\n\u003cp\u003e4) Using the results of the cyclostratigraphic analysis, we developed a refined model of cyclic carbonate deposition in the Late Triassic Dachstein platform and demonstrated that aquifer- and limno-eustasy are the most likely drivers of cyclic sea level changes that transcribed the orbitally driven climate changes into the sedimentary record.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e5) Variations in the genesis and preservation of the Lofer cycles led to differences in their completeness, resulting in complete, depositionally incomplete, erosionally truncated, and incomplete and truncated types. We show here, for the first time, that cycle completeness is also orbitally controlled and is especially sensitive to long eccentricity forcing. An additional, tentative but intriguing observation is that changes in the variance in cycle types may be paced by the 1.2\u0026ndash;1.3 Myr grand orbital cycle.\u003c/p\u003e\n\u003cp\u003e6) The spectral analysis also revealed several sub-Milankovitch cycles, of which the 13.5, 7, 5, 3.4, 2.4, and 1.48 kyr cycles are the most prominent. We discuss their possible driving forces and support the views that many of the sub-Milankovitch cycles that were originally discovered in the Quaternary records could also be detected in the Mesozoic, despite the contrast between icehouse and greenhouse climate regimes.\u003c/p\u003e\n\u003cp\u003e7) Comparison with other studies of Upper Triassic Lofer cyclic successions from the extensive Dachstein platform system points to close similarities in the thickness of individual Lofer cycles, the periods of all identified cycles, and the sedimentary rates, that points to common allocyclic processes. Taken together, these findings provide definitive evidence for the orbital forcing of carbonate sedimentation in the Late Triassic Dachstein platform system.\u003c/p\u003e"},{"header":"Declarations","content":"\u003cp\u003eAcknowledgements\u003c/p\u003e\n\u003cp\u003eWe thank Dorottya D\u0026eacute;nes for digitizing the original core log and \u0026Aacute;d\u0026aacute;m Kocsis for providing a paleogeographic base map. This study was supported by the \u0026Uacute;NKP-23-3 New National Excellence Program of the Ministry for Culture and Innovation from the source of the National Research, Development and Innovation Fund to ZV and by the National Research, Development and Innovation Fund Grant K135309 to JP.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eFunding\u003c/strong\u003e This study was supported by the \u0026Uacute;NKP-23-3 New National Excellence Program of the Ministry for Culture and Innovation from the source of the National Research, Development and Innovation Fund to ZV and by the National Research, Development and Innovation Fund Grant K135309 to JP.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eCompeting interests\u003c/strong\u003e The authors have no competing interests to declare that are relevant to the content of this article.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\n\u003cli\u003eBALLA, Z. 1982: Development of the Pannonian basin basement through the Cretaceous-Cenozoic collision: A new synthesis. \u0026mdash; \u003cem\u003eTectonophysics\u003c/em\u003e \u003cstrong\u003e88,\u003c/strong\u003e 61-102. http://doi.org/10.1016/0040-1951(82)90203-7 \u003c/li\u003e\n\u003cli\u003eBALOG, A., HAAS, J., READ, F. \u0026amp; Coruh, C. 1997: Shallow marine record of orbitally forced cyclicity in a Late Triassic carbonate platform, Hungary. \u0026mdash; \u003cem\u003eJournal of Sedimentary Research\u003c/em\u003e \u003cstrong\u003e67,\u003c/strong\u003e 661\u0026ndash; 675.\u003c/li\u003e\n\u003cli\u003eBEAUFORT, L. 1994: Climatic importance of the modulation of the 100 kyr cycle inferred from 16 m.y. long Miocene records. \u0026mdash; \u003cem\u003ePaleooceanography\u003c/em\u003e \u003cstrong\u003e9/6,\u003c/strong\u003e 821-834. http://doi.org/10.1029/94PA02115 \u003c/li\u003e\n\u003cli\u003eBERGER, A. \u0026amp; LOUTRE, M.F. 1997: Intertropical latitudes and precessional and half-precessional cycles. \u0026mdash; \u003cem\u003eScience\u003c/em\u003e \u003cstrong\u003e278,\u003c/strong\u003e 1476-1478. http://dx.doi.org/10.1126/science.278.5342.1476 \u003c/li\u003e\n\u003cli\u003eBERGER, A., LOUTRE, M. 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However, despite a long history of study, their allocyclic vs autocyclic origin remains controversial. Using modern cyclostratigraphic methodology, here we revisit the archive data of the Dachstein Limestone in core Po-89 from the Transdanubian Range, Hungary. Analysis of high-resolution time series of the Lofer facies types, colour, greyscale, and lithology revealed several spectral peaks that are identified with the Milankovitch cycles. The Lofer cycles correspond to a robust peak with a period of 3.6 m that is the expression of precession cycles with a period 21.65 kyr. The sedimentary rate is 16.5 cm/kyr, thus the studied core section represents 2.5 Myr. Our model of cyclic carbonate deposition suggests that aquifer- and limno-eustasy were the most likely drivers of cyclic sea level changes. Differences in the depositional processes and preservation of the Lofer cycles led to variations in their completeness that is also orbitally controlled and responds primarily to long eccentricity forcing. We detected several sub-Milankovitch cycles, of which the 13.5, 7, 5, 3.4, 2.4, and 1.48 kyr cycles are the most prominent. Our results are in good agreement with other studies of Upper Triassic Lofer cyclic successions. The similarities in the thickness of individual Lofer cycles, the periods of all identified cycles, and the sedimentary rates suggest common allocyclic processes. Our findings provide definitive evidence for the orbital forcing of carbonate sedimentation in the Late Triassic Dachstein platform system.","manuscriptTitle":"Definitive orbital control on the origin and preservation of Lofer cyclicity in the Late Triassic Dachstein platform","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2024-04-30 19:02:11","doi":"10.21203/rs.3.rs-4281587/v1","editorialEvents":[{"type":"communityComments","content":0}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"1d3250cb-664b-43f1-89b3-ee50fe471e09","owner":[],"postedDate":"April 30th, 2024","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"published-in-journal","subjectAreas":[],"tags":[],"updatedAt":"2025-12-08T20:08:41+00:00","versionOfRecord":{"articleIdentity":"rs-4281587","link":"https://doi.org/10.1016/j.palaeo.2025.113365","journal":{"identity":"palaeogeography-palaeoclimatology-palaeoecology","isVorOnly":true,"title":"Palaeogeography, Palaeoclimatology, Palaeoecology"},"publishedOn":"2025-10-27 00:00:00","publishedOnDateReadable":"October 27th, 2025"},"versionCreatedAt":"2024-04-30 19:02:11","video":"","vorDoi":"10.1016/j.palaeo.2025.113365","vorDoiUrl":"https://doi.org/10.1016/j.palaeo.2025.113365","workflowStages":[]},"version":"v1","identity":"rs-4281587","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-4281587","identity":"rs-4281587","version":["v1"]},"buildId":"qtupq5eGEP_6zYnWcrvyt","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}