Wan Yang , Dan J.Lehrmann

1.Geology and Geophysics Program, Missouri University of Science and Technology, Rolla, Missouri 65409, USA 2.Department of Geosciences, Trinity University, San Antonio, TX 78212, USA

1 lntroduction＊

Shallowing-upward peritidal carbonate cycles result from interplay of allogenic and autogenic processes controlling accommodation space and sediment accumulation(e.g., Goldhammeret al., 1990, among many others).The former is controlled by eustasy and subsidence (e.g., Read and Goldhammer, 1988), the latter by factors affecting carbonate productivity and sediment redistribution, such as water depth, biota, salinity, oxygenation, nutrient, and current energy (cf.Tuckeret al., 1990; Schlager, 2005).Three mechanisms, all assuming constant subsidence and sedimentation, are commonly suggested for peritidal cycle formation: composite eustasy (e.g., Goldhammeret al.,1990), tidal flat sediment accumulation and progradation(e.g., Ginsburg, 1971; Pratt and James, 1986), and random processes (e.g., Spencer and Demicco, 1989; Drummond and Wilkinson, 1993a; Wilkinsonet al., 1999; Burgess,2001, 2008), among which only Milankovitch-related composite eustasy can generate multi-order hierarchical cycles.In this study, we explore the link between carbonate productivity and cyclicity on the basis of sedimentary and quantitative evidence of peritidal cycles in South China.

2 Characteristics of peritidal carbonate cycles

The peritidal carbonate cycles described here are suitable to explore the role of carbonate productivity variations on peritidal cyclicity, because they developed during the Early Triassic (Induan)greenhouse period when eustasy was minimal (Frakeset al., 1992; Scoteseet al., 1999)and the benthic biota recovering from the end-Permian mass extinction was highly sensitive to varying oceanic conditions.They were deposited on an isolated flat-topped carbonate bank, which covers 10×70 km2in the eastern Paleo-Tethys (Figure 1A, 1B; Lehrmannet al., 1998).It was named as the Great Bank of Guizhou by Lehrmann(1993)and as the Luodian Carbonate Platform by Fenget al.(1997).The bank has a low-relief profile with oolite shoals at the margin, shallow-subtidal and peritidal deposits in the interior, and pelagics, debris-flow deposits and turbidites on gentle basin-margin slopes (Figure 1C).Interior strata are 265 m thick beginning in the lowermost Triassic withRenalcisbiostromes, followed by lime mudstone, oolite, and cyclic peritidal carbonate.

The cyclic carbonate is Olenekian in age.Two sections,Dajiang (DJ)on the windward side and Dawen (DW)toward the leeward side, are 140 m and 162 m thick, respectively (Figure 1C).They contain a total of 149 cycles that range from 0.2 to 7.4 m thick and are 2 m thick on average(Figures 1C, 2A, 2B).A typical cycle consists of four facies (Figure 2C; Lehrmannet al., 1998, 2001): subtidal skeletal packstone or oolitic grainstone in the lower part,calcimicrobialRenalcismound or biostrome facies in the middle, and intertidal flaser-bedded ribbon-rock facies in the upper part, all of which are pyritiferous.The skeletal packstone and reef mounds contain a low-diversity biota of cyanobacteria, echinoderms, bivalves, gastropods, lingulid brachiopods, spirorbids, and ostracodes.Ribbon rocks contain alternating lime mud and fine peloidal packstone and grainstone laminae, scour surfaces, ripple crosslamination, lime-mud drapes, and minor prism cracks.Rarely, cycles are capped by supratidal microbial laminite facies, which account for only 2% of the section thickness.Overall, the facies were deposited in a dominantly lowenergy, restricted- to normal-marine peritidal environment.The facies stacking suggests a shallowing-upward trend of depositional environments within each cycle, upward from high-energy shallow subtidal, relatively deep low-energy subtidal, to intertidal and, rarely, supratidal(see Lehrmannet al., 1998, 2001 for thorough descriptions and interpretations).

Furthermore, cycle (parasequence)stacking patterns show gradual increase and decrease of cycle thickness, defining a third-order sequence boundary and several fourthorder cycle sets that correlate between DJ and DW sections (Figures 2, 3A; Lehrmannet al., 2001).Lehrmannet al.(2001)stated that the cycle stacking patterns are similar to those of lower Paleozoic green-house sequences and different from those of ice-house sequences.They concluded that facies similarities such asRenalcismound and flaser-bedded intertidal ribbon rock reflect anomalous oceanic conditions resulting in low biodiversity and low intensity of bioturbation after the end-Permian extinction.Similarities in cycle stacking patterns reflect low-amplitude, high-frequency sea-level fluctuations resulting from greenhouse conditions common to the Early Paleozoic and Early Triassic.

The three-order hierarchical stratigraphic relationship as suggested by Lehrmannet al.(2001)was quantitatively tested by Yang and Lehrmann (2003)through time series and spectral analysis of cycle thickness and facies data of DJ and DW sections (Figure 4).Milankovitch climatic signals of prominent short-eccentricity (94.9-131.2 kyr),short-obliquity (35.8 kyr), and long precessional index(21.2 kyr), and minor long-eccentricity (412.9 kyr), longobliquity (45.3 kyr), short precessional index (17.7 kyr),and a constructional-tone (9.7 kyr)were detected.The estimated stratigraphic completeness is much greater than that of icehouse stratigraphic records.The results suggest that Milankovitch climatic forcing had greatly influenced sedimentation.Yang and Lehrmann (2003)speculated that variations in carbonate productivity and environmental conditions driven by Milankovitch climatic forcing, combined with low-amplitude sea-level fluctuations,were likely major controls on cyclic sedimentation.Furthermore, evolutive spectra of the two sections show that dominant Milankovitch climatic forcings varied from short eccentricity, obliquity, to long-precessional index during the course of sedimentation, suggesting variations in the type and magnitude of oceanic and climatic processes and their mechanisms during the course of cyclic sedimentation of DJ and DW sections.Finally, the DW and DJ cycles accumulated during the Early Triassic aftermath of end-Permian mass extinction.This period is characterized by extremely low biodiversity, a molluskdominated skeletal biota, low skeletal abundance, extremely small and lightly calcified fauna (e.g., Payneet al., 2006), and microbial and cement precipitates (e.g.,Woodset al., 1999; Lehrmannet al., 2003; Payneet al.,2007).A decimated carbonate productivity potential and detrimental environmental conditions (e.g., anoxia and euxinia)had been the norm during the delayed recovery from the extinction (e.g., Payneet al., 2004).The lithologic and stratigraphic characteristics and the controlling processes and mechanisms of the DW and DJ cyclicity can be better understood in this global and temporal context as discussed below.

Figure 1 A-Paleogeographic location of Yangtze Block at ～12°N latitude, which migrated across the paleoequator from the end of Permian to the Early Triassic.Modified from Scotese (1994); B-Early Triassic paleogeography of Nanpanjiang Basin compiled from regional geologic maps by Bureau of Geology and Mineral Exploration and Development of Guizhou Province (1987)and Bureau of Geology and Mineral Resources of Guangxi Zhuang Autonomous Region (1985), showing location of the Great Bank of Guizhou or Luodian Carbonate Platform; C-Restored Lower Triassic cross-section of the bank, showing stratigraphic architecture and location of Dawen and Dajiang sections.See B for location.After Lehrmann et al., 2001.

Figure 2 Lithostratigraphic columns of Lower Triassic strata in Dawen (A)and Dajiang (B)sections.Three orders of cycles,namely parasequences, parasequence sets, and depositional sequences, were identified.Systems tracts and sequence boundary of depositional sequences are indicated.TST = transgressive systems tract; HST = highstand systems tract; SB = sequence boundary; m = mudstone; w = wackestone; p = packstone; g = grainstone; dashed line indicates tentative correlation.The typical or“ideal” parasequence is shown in C.Modified from Lehrmann et al., 2001.Facies ranks interpret relative water depth of component lithofacies.

Figure 3 Variations in thickness (A)and component facies (B)of the Dawen (DW)and Dajiang (DJ)sections (Figure 1C).The average and range of cycle thickness are 2.0 m and 0.2-7.1 m for DW and 2.1 m and 0.25-7.4 m for DJ.Left panel: Cycle thickness pattern of cycle bundles in a depositional sequence of the DW section shows a three-order hierarchy and is correlative to the DJ section (Lehrmann et al., 2001).Right panel: Subtidal and intertidal facies dominate, with rare supratidal facies in the upper part of the sections.The facies curves were used in spectral analysis of Yang and Lehrmann (2003).Lines between two sections are correlation lines, dashed where it is tentative.“sub”,“int”, and “sup” represent subtidal, intertidal, and supratidal facies, respectively.

Figure 4 Spectra of Dajiang (A)and Dawen (B)sections time series.Thick lines are spectra; thin lines below the spectral lines are lower than 90% confidence limits; thin vertical lines above the spectral lines are Milankovitch line spectra at 247 Ma (Berger et al.,1992).Nyquist frequency is 25 for Dajiang and 20 for Dawen spectra.Thickness-time conversion, spectral analysis, and period calibration were conducted separately for the two sections.See Yang and Lehrmann (2003)for details.The calibrated spectra contain prominent short-eccentricity, short-obliquity, and long-precession index peaks, and minor long-eccentricity, long-obliquity, short-precession index, and constructional-tone peaks.Thus, Milankovitch climatic forcing probably greatly influenced cyclic sedimentation of DJ and DW sections.

3 Carbonate productivity variations

Intra- and inter-cycle variations in carbonate productivity are interpreted from facies type, thickness, stacking pattern, and estimated sedimentation rate of DJ and DW cycles.Intertidal and supratidal sediments are mainly transported from the subtidal factory and redistributed on the tidal flat.Large subtidal production will likely generate copious sediments to quickly fill the accommodation space, resulting in shallowing-upward subtidal-intertidalsupratidal successions, whereas small production results in thin intertidal and supratidal facies or absence of these facies, assuming the rate of accommodation space generation is constant.Sea-level change was minimal during the Early Triassic because of the absence of continental glaciers; and the subsidence of the platform was approximately constant at a cycle scale.Thus, the rate of accom-modation space generation on the bank was relatively constant.As a result, facies type and thickness of DJ and DW cycles are first-order indicators of carbonate productivity,even though sediment redistribution and preservation may affect facies type and thickness.

Several lines of evidence from the DJ and DW cycles provide clues on benthic carbonate productivity and its intra-cycle variations.First, the low-diversity biota of cyanobacteria, echinoderms, bivalves, gastropods, lingulid brachiopods, spirorbids, and ostracodes, and the low abundance of skeletal grains (Payneet al., 2006)suggest low carbonate productivity.Ooid production in the marginal shoals was high enough to export ooids to the interior(Figures 1C, 2; Lehrmannet al., 2001).However, oolitic facies are thin and uncommon (0.9 m thick on average;14% in total thickness), suggesting that chemical precipitates were subordinate to skeletal and mound sediments,which are 1.3 m thick on average.Second, the effective accumulation rate of subtidal facies is 31-24 cm/ky, an order of magnitude higher than that (6-3 cm/ky)of combined intertidal and supratidal facies, as estimated by Yang and Lehrmann (2003)on the basis of Milankovitch cycle period calibration.The rates indicate decreased productivity during intertidal and supratidal deposition (Figure 5).

Third, the intertidal facies is thin, 0.5 m thick on average (Figure 3).The supratidal facies is not only thin, 0.7 m thick on average, but also rare, only presents in 14 out of 149 cycles.These facts indicate common termination of intertidal deposition before the available intertidal and supratidal space was filled.The termination may have four causes: subaerial exposure due to a sea-level fall, drowning by a sea-level rise, some unknown random processes,or a productivity shutdown due to environmental stress(Tuckeret al., 1990; Schlager, 2005).Thick intertidal and supratidal facies commonly occur during tidal flat progradation accompanying a sea-level fall.Thus, the thin intertidal facies and rare supratidal facies suggest that a sealevel fall during intertidal and supratidal deposition likely did not occur.The fall, if it occurred, was likely short and minimal, as indicated by the absence of prolonged subaerial exposure on subtidal facies.A small sea-level rise is also not likely, because it will not be able to drown the platform; on the contrary, it may increase carbonate productivity in the interior (Schlager, 2005).Any random processes, such as episodic subsidence, will not generate cycle hierarchy.Thus, a drastic reduction of sediment productivity in the subtidal factory caused by environmental stresses during intertidal deposition is the only plausible mechanism causing the termination of intertidal deposition and rarity of supratidal facies.

Inter-cycle variations in cycle and facies thickness and facies type indicate long-term environmental and productivity changes (Figures 2, 3; cf.Drummond and Wilkinson,1993b; Lehrmannet al., 1998, 2001; Yang and Lehrmann,2003).The occurrence of supratidal facies in the middle and upper DW and DJ sections, although rare, coincides with limited taxonomic recovery and, perhaps, pulses of increased productivity during the Induan (e.g., Kozur,1998; Twitchettet al., 2004; Chenet al., 2007).There are also systematic upsection changes in the proportions of ooids, calcimicrobial mud, and skeletal grains.The evolving Milankovitch signal upsection correlates with changes in cycle thickness and facies type.For example, in DW section, the 0-60 m segment contains a mixture of thick to moderately thick cycles (Figures 2, 3); and some of the thick cycles are probably bundles of thin cycles.This is reflected in a dominant eccentricity signal in the evolutive Milankovitch spectrum (see Yang and Lehrmann, 2003,for evolutive spectra of DJ and DW sections).The 40-80 m segment contains predominantly thin cycles of approximately equal thickness and abundant oolites.This is reflected in a dominant obliquity signal.The occurrence of both thick and very thin cycles in the 100-140 m segment is reflected by co-existing precessional index and short-eccentricity signals.The occurrence of thin but approximately equal thickness cycles in the 120-160 m segment is reflected by the dominant precessional index and a minor constructional tone signal (Figures 2, 3; Yang and Lehrmann, 2003).Finally, the 60-100 m segment in the middle DW section contains mixed thin and moderately thick cycles and covers the stratigraphic turning point from the upper highstand systems tract to the lower transgressive systems tract across a sequence boundary (Figures 2, 3).The spectrum of this segment has a broad peak centered on the obliquity band, probably as a result of mixing of obliquity in the lower part and precessional index in the upper part.

The above discussions on intra- and inter-cycle variations of facies type and cycle and facies thickness, as well as their correlation with Milankovitch climatic forcings,suggest a cause-effect relationship between Milankovitch climatic forcing and multi-order cyclic sedimentation in a greenhouse climate in an equatorial mid-ocean setting.However, the oceanographic and sedimentary mechanisms that link climatic forcings with stratigraphic characteristics of DW and DJ cycles are not clear (Yang and Lehrmann,2003).For example, orbital eccentricity and obliquity are physically independent, whereas the precessional index ismodulated by the eccentricity (Berger, 1977, 1988; Bergeret al., 1992; cf.Liuet al., 2000)and, thus, the climatic forcings affected and interacted with geologic processes nonlinearly (e.g., Ripepe and Fischer, 1991; deMenocal,1995).Formation, distribution, and deposition of oolitic sediments are closely related to climatic and oceanic conditions that affect the energy and water chemistry of the windward platform margin.The frequency and strength of tropical storms would affect the extent and thickness of oolite spill-over lobes into the platform interior (Figure 1C).Plate reconstructions place the study area at 12°N latitude facing N45°E into the northeast trade winds (Figure 1; Kutzbachet al., 1990; Crowley, 1994; Scotese, 1994;Scoteseet al., 1999).Thus, obliquity forcing may have been transferred to the sedimentary record via equatorial atmospheric circulation (cf.Crowley, 1994).

Figure 5 Speculations on temporal variations of facies and relationships among subtidal sediment productivity, environmental factors, and eustasy during the deposition of an ideal Dawen and Dajiang cycle.Environmental perturbations in the subtidal zone may be the main cause of intra-cycle productivity variations in a greenhouse climate when eustasy was minimal, as indicated by the common termination of intertidal deposition, rarity of supratidal facies, and lack of prolonged subaerial exposure in those cycles.

Furthermore, the upsection spectral shift in Milankovitch climatic forcings in the DW and DJ records suggests that no one mechanism dominated through the entire course of sedimentation.If the evolving Milankovitch signals were mainly caused by an estimated 6°-7°northward plate movement during the Olenekian, the latitudinal climatic gradient in the eastern Tethys must have been very steep, conforming with a similar interpretation from the low-latitude continental record in Late Triassic western Pangea (Kent and Olsen, 2000).The other possible scenario is that, assuming the amount of plate movement is insignificant during the Olenekian, the evolving Milankovitch climatic forcing may have been caused mainly by dynamic changes of global atmospheric and oceanic conditions.Temporal changes of dominant Milankovitch climatic forcing at a given locality were documented in continental northwestern Africa in the Plio-Pleistocene(e.g., deMenocal, 1995), and should have been common in geological records (Berger, 1988; see Hinnov and Park,1998; Meyerset al., 2001; P?likeet al., 2001 for more examples)because of the complex interaction of atmospheric and oceanic systems (e.g., Crowley, 1994).The above speculations on paleoclimatic and oceanographic changes suggest that sedimentary processes and mechanisms other than sea-level fluctuations may have played a major role in cyclic sedimentation in the study area.Some specific mechanisms are speculated in the following sections.

4 Factors controlling carbonate pro?ductivity variations

Factors affecting subtidal carbonate productivity on the Great Bank of Guizhou include salinity, possible incursions of toxic anoxic and euxinic waters, nutrient levels, and water depth.Each factor is considered separately below.

First, the slowly-recovering biota was sensitive to salinity variations of the bank water (Figure 5).Salinity changes due to varying evaporation that was induced by sea-surface temperature changes were likely minimal, because temperature varied little in the low-latitude ocean and equable greenhouse climate (Kutzbach, 1994).However, hyposalinity prevailed in the bank interior during periods of high rainfall of the megamonsoonal climate overthe Tethys (Kutzbach and Gallimore, 1989; Parrish, 1993;Crowley, 1994).Rainfall may have varied 33% in the lowlatitude east coast in a precession cycle (Kutzbach, 1994);and peak temperature on land correlated with maximum rainfall and hyposalinity in coastal regions due to precessional forcing modulated by 100 ky cycles in the Early Triassic (Crowley, 1994).Varying monsoon intensity at the precessional and eccentrical scales would have caused rainfall and, thus, intra-cycle salinity variations.Hence, intertidal deposition occurred during periods of low rainfall and high carbonate productivity, followed by nondeposition during periods of high rainfall and low productivity.In addition, the greater proportion of supratidal facies in the upper sections (Figures 2, 3)indicates an increase in carbonate production, probably related to a long-term reduction of monsoon intensity, more saline marine water,and enhanced carbonate productivity in response to northward migration of the South China Plate across the equator to ～15°N from 240-250 Ma (Kutzbach, 1994; Scotese,1994).

Second, toxic deep anoxic waters, also loaded with CO2and H2S, may have poisoned the benthos.Although the causes of the end-Permian extinction are still debatable, there is general agreement that deep oceanic waters were anoxic and likely also euxinic and charged with CO2throughout the Early Triassic (Hallam, 1991; Schubert and Bottjer, 1995; Knollet al., 1996; Wignall and Hallam,1996; Wignall and Twitchett, 1996; Isozaki, 1997; Heydariet al., 2000; Payneet al., 2004; Kumpet al., 2005; Meyeret al., 2008).Meyer and Kump’s (2008)results of Earth system modeling support a link between oceanic nutrient status and the redox state of the end-Permian ocean.Modest increases in marine phosphate concentration can result in widespread deep ocean euxinia.Hydrogen sulfide built up in the Paleo-Tethys Ocean relative to the Panthalassic Ocean due to nutrient-trapping ocean circulation in the Paleo-Tethys.These toxic bottom waters, when delivered to the banktop, would have decimated benthic biota and drastically reduced benthic carbonate productivity and sediment production.

The delivery mechanisms include rising of the toxic waters in the water column via upwelling, mixing and/or overturn of deep to surface water masses, and small fluctuations of sea level causing toxic floodings.Recent modeling of Meyer and Kump (2008)and Meyeret al.(2008)suggested that upwelling delivered deep sulfidic waters to the photic zone in the eastern Paleo-Tethys in Guizhou and the preferential buildup of nutrients in the restricted Tethys greatly exacerbated euxinia in the region.In addition, mixing may have occurred due to intensified oceanic upwelling and downwelling caused by, for example, global seasonality variations and increased equator-to-pole temperature gradient related to the obliquity forcing (Kutzbach and Gallimore, 1989; Kutzbachet al., 1990; Kutzbach, 1994;Wignall and Twitchett, 1996; Parrishet al., 2001).Wignall and Twitchett (1996)documented anoxic flooding above storm wavebase (see also Kozur, 1998)and fluctuations of anoxic, dysaerobic, and oxic conditions on the Early Triassic platforms in western Tethys.Similarly, seafloor aragonite fans suggest upwelling of anoxic, alkaline waters in the Early Triassic shelf and slope of the western Pangea(Woodset al., 1999).

The study area in the low-latitude eastern Tethys was prone to toxic water flooding onto the shelf where strong ocean currents were common (Kutzbachet al., 1990).Repeated incursions of toxic water masses over the banktop were facilitated by transgressions during or shortly after intertidal deposition and caused termination of intertidal deposition and absence of supratidal facies, or even entire intertidal facies in 11 of a total 149 DW and DJ cycles(Figure 5).After termination, subtidal deposition gradually resumed in the space created by continued subsidence and, possibly, a sea-level rise.As a result, the subtidal facies overlie the intertidal facies without a prominent exposure surface.The rarity of supratidal facies, lack of prominent subaerial exposure surfaces, and correlative cycles of DW and DJ sections (Figures 2, 3; Lehrmannet al., 2001)support this interpretation that banktop flooding of toxic waters poisoned the benthic biota, causing a great reduction in carbonate productivity.Finally, the varying precessional and obliquitous signals on the DW and DJ evolutive spectra (Yang and Lehrmann, 2003)suggest alternating sluggish and active oceanic circulation, which would have induced hierarchical variations of carbonate productivity at the Milankovitch cycle scale.

Third, excessive nutrients in the water (e.g., Meyer and Kump, 2008)will suffocate benthos to reduce carbonate productivity (Figure 5; Hallock and Schlager, 1986).The superanoxia of Early Triassic oceans (e.g., Isozaki, 1997)also suggests a high overall primary productivity in Panthalassa.But the DW and DJ rocks are not enriched in organic matter and phosphate (cf.Woodset al., 1999; Parrishet al., 2001).However, the recurring growth of calcified microbialite in these cycles was likely stimulated by pulses of increased nutrients (cf.Lehrmann, 1999; Lehrmannet al., 2001).Further geochemical work is needed to evaluate the possibility of excess nutrients and potential linkage with upwelling.If there were significant pulses of excessnutrients to the banktop, cycling of organic matter or other factors may have inhibited organic matter preservation in the sediment.

Last, eustasy may have changed the water depth and,thus, the subtidal productivity on the platform (Figure 5;e.g., Pittetet al., 2000).Shoaling, subsidence, and nonglacial eustasy (Kutzbach, 1994; Scoteseet al., 1999)all affect water depth.Non-glacial eustasy of several to a few tens of meters (e.g., Cisne and Gildner, 1988)can be driven by Milankovitch forcing via changing continental water storage (Jacobs and Sahagian, 1993), the Earth’s internal responses to orbital variations (M?rner,1994), and thermal ocean expansion (Schulz and Sch?fer-Neth, 1997; see also Pindell and Drake, 1998).Eustasy affected accommodation space and, thus, the cycle thickness.But the rare supratidal facies and vadose meteoric alteration, and the lack of prominent subaerial exposure surfaces directly on subtidal facies indicate a minimal effect.A small sea-level rise will deepen the subtidal zone and slightly increase carbonate productivity.More likely,the rise would aid the platform with flooding of anoxic and/or CO2-charged deep water.

5 Productivity?driven cyclic peritidal carbonate sedimentation

We propose a conceptual model that explains how temporal variations in carbonate productivity alone can formshallowing-upward peritidal cycles under constant subsidence and sea level (Figure 6).The productivity varies in four phases from non-productive, gradual increase, peak,to rapid decline; and a lag time is included in the non-productive phase (cf.Readet al., 1986).If subtidal carbonate productivity is proportional to production of carbonate sediments, the model produces shallowing-upward cycles dominated by subtidal and intertidal facies, and cycles containing only subtidal facies or subtidal-supratidal facies when productivity is extremely low or high, respectively (Figure 6).Adding small sea-level changes in the model slightly changes depositional space without altering the overall stratigraphic pattern.Lateral variations in accommodation space, productivity, and sediment redistribution on the platform (e.g., Pratt and James, 1986;Osleger, 1991)related to topography and type of benthos will also cause autogenic variations in the type, timing,and amount of sediment accumulation.The stratigraphic hierarchy of the DW and DJ successions, however, suggests these variations are secondary.The conceptual model shows how subtidal carbonate productivity variations induced by Milankovitch-related climatic and oceanographic processes may have formed the hierarchical facies and thickness patterns of DW and DJ cycles.

Figure 6 A one-dimensional conceptual model of peritidal cyclic sedimentation under constant sea level and subsidence, and fluctuating carbonate productivity.The productivity variations in the subtidal zone are ordered and mainly caused by environmental perturbations induced by Milankovitch climatic and oceanographic processes.During minimal productivity, deposition on the tidal flat ceases,terminating intertidal or even subtidal deposition to form a nondepositional hiatus; in the meanwhile, subsidence is creating more depositional space.During a gradual productivity increase, the space is slowly filled to form the lower subtidal facies.During peak productivity, sediments fill the subtidal and intertidal space.The subtidal space is only partially filled if the peak production is low; the supratidal space is filled if the peak is high.During a sharp productivity decline, sediment accumulation is minimal.This model shows that meter-scale peritidal carbonate cycles can be formed by productivity variations alone.Adding small sea-level fluctuations (not shown)will accentuate depositional space variations without affecting the general stratigraphic pattern.

The productivity-driven succession has a high stratigraphic completeness.Yang and Lehrmann (2003)estimated a 36%-75% and 47%-98% completeness for DW and DJ sections, respectively, which is high in comparison to 10%-20% for Phanerozoic peritidal carbonate cycles(Sadler, 1994)and 3%-30% for Paleozoic peritidal carbonate cycles (Wilkinsonet al., 1991; Yanget al., 1995).The high completeness is attributed to the small eustasy and may be characteristic of productivity-driven greenhouse peritidal cycles.

This model demonstrates that the formation of greenhouse carbonate cycles (e.g., Goldhammeret al., 1990;Zempolich, 1993; among many others)may not require eustasy of several tens of meters.The autocyclic model of Goldhammeret al.(1990)assumed no 4thand 5th-order eustasy but constant subtidal sedimentation regulated by lag depth, which, in fact, causes productivity variations by shutting down the subtidal carbonate factory when the platform was within the lag depth.The biota in the study area was particularly vulnerable to environmental perturbations.The cyclicity observed in other carbonate platforms may also reflect primary influence of fluctuating carbonate productivity.However, in cases of a robust biota that can produce copious sediments to quickly fill the accommodation space, peritidal sedimentation would be mainly controlled by eustasy.In all cases, productivity variations always exist and should be considered in interpreting cyclic carbonate sedimentation.

Acknowledgements

We thank S.Mazzullo, K.Meyer, E.Rankey, B.Wilkinson, and Mei-Yi Yu for discussions, and the late R.Goldhammer, D.Bosence, P.Burgess, D.Pollit, E.Rankey, W.Schlager, and N.Tabor for insightful reviews of the early drafts.We appreciate the constructive comments from Journal of Palaeogeography reviewers Professor Ming-Xiang Mei and Professor Zeng-Zhao Feng, which improved the quality of the paper.

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