USING ELEMENTAL CHEMOSTRATIGRAPHY ON MID-LATE FRASNIAN PLATFORM-TOP SUCCESSIONS FROM THE LENNARD SHELF OUTCROPS, CANNING BASIN, WESTERN AUSTRALIA
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Kenneth Ratcliffe, Ted E. Playton, Paul Montgomery, David Wray, Samuel Caulfield-Kerney, Eric Tohver, Roger M. Hocking, Peter W. Haines, Joseph Kirschvink, Maodu Yan, 2017. "USING ELEMENTAL CHEMOSTRATIGRAPHY ON MID-LATE FRASNIAN PLATFORM-TOP SUCCESSIONS FROM THE LENNARD SHELF OUTCROPS, CANNING BASIN, WESTERN AUSTRALIA", NEWADVANCES IN DEVONIAN CARBONATES: OUTCROP ANALOGS, RESERVOIRS AND CHRONOSTRATIGRAPHY, Ted E. Playton, Charles Kerans, John A.W. Weissenberger
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High-resolution chronostratigraphic correlation using elemental chemostratigraphy in platform carbonates is typically difficult to achieve. Here, elemental chemostratigraphy is used to correlate between two platform-top, carbonate-dominated field sections from the narrow Lennard Shelf that existed on the NE margin of the Canning Basin, Western Australia, during the mid-late Frasnian. The correlation, constrained by magnetic polarity reversals and physical ground truthing, is based on recognition of distinctive cyclical “stacking patterns” defined by changes in concentrations of the trace element zirconium (Zr). Zr concentrations are controlled by the amount of the heavy mineral zircon in the sediments, which is derived from a terrigenous source and is diagenetically very stable. The stacking patterns in the lower part of the study sections display gradually upward-increasing values of Zr to a maximum, followed by an almost immediate fall to a minimum. In the upper part of the study interval, the cycles are more symmetrical, with both gradually increasing and decreasing portions. The point at which the change in Zr stacking pattern occurs in the two sections is synchronous and occurs in association with a supersequence maximum flooding surface. The correlation based on maximum and minimum Zr values throughout the two sections is demonstrated to be chronostratigraphic by comparison with correlations based upon paleomagnetism and physical ground truthing.
When element ratios commonly used as provenance and paleoclimate proxies are plotted, the variations between closely spaced samples are greater than any systematic variations throughout the study intervals. Therefore, no isochemical chemozones can be defined, implying that during deposition of the study intervals, there were no long-lived changes in sediment provenance or paleoclimate that the elemental chemistry can detect.
The work presented here shows that the standard approach of defining isochemical chemozones for chemostratigraphic correlation is not always appropriate. However, an approach using cyclical changes in elemental variables for chemostratigraphic correlation between two closely spaced sections is chronostratigraphically valid. The greater challenge is in application of the same approach to more widely spaced sections, potentially in different facies of a carbonate setting.
Chemostratigraphy, as used in this study, refers to the definition of stratigraphic units or surfaces using variations in whole-rock elemental concentrations. Typically, the aim of this chemostratigraphic approach is to identify elements and element ratios that change through time and that enable sediments of the same age to be correlated, or to differentiate sediments that are asynchronous. Published accounts of chemostratigraphy are largely from petroleum basins, mostly investigating fluvial siliciclastic systems and shale resource plays. In fluvial settings, the elemental data are typically used to recognize changes in paleoclimate (Pearce et al. 2005, Ratcliffe et al. 2010), changes in sedimentary facies, and changes in sediment provenance (Ehrenberg and Siring 1992, Armstrong-Altrin et al. 2004, Pe-Piper et al. 2008, Hildred et al. 2010, Wright et al. 2010, Ramkumar et al. 2011, Ratcliffe et al. 2015). In shale resource plays, the elemental data are commonly used to recognize terrigenous material influx and content (Algeo et al. 2004, Soua 2010, ver Straeten et al. 2011, Whalen et al. 2015) and as a proxy for bottom water conditions during deposition (Tribovillard et al. 2006, Rowe et al. 2012, Tinnin et al. 2013). These changes are then used to build a stratigraphic framework and provide stratigraphic correlations.
Published studies using elemental data on carbonate-dominated successions for stratigraphic correlation remain relatively uncommon. They often concentrate on elements associated with carbonate fraction (Pearce and Jarvis 1995, Jarvis et al. 2001, Wray and Gale 2006, Mabrouk et al. 2007, Callonnec et al. 2014, Coimbra et al. 2015), rather than the major and trace element signatures associated with terrigenous contents (Stüben et al. 2005; Śliwiński et al. 2012; Davies et al. 2013, 2014; Craigie 2015). Work published on carbonate chemostratigraphy commonly notes that the cyclical variation in elemental compositions can be recognized on chemical logs (Mabrouk et al. 2007, Montgomery et al. 2011, Davies et al. 2013, Craigie 2015). Authors relate the cyclical variations to changes in the amount of terrigenous material in the carbonates (Montgomery et al. 2011, Davies et al. 2013) and to base-level fluctuations (Mabrouk et al. 2007, Davies et al. 2013, Craigie 2015). Cyclical fluctuations in terrigenous content that relate to base-level fluctuations in carbonate sediments are also commonly recognized from magnetic susceptibility studies (Ellwood et al. 2008, 2013; Da Silva et al. 2009; Whalen and Day 2010; Śliwiński et al. 2012) and in some mudrock studies (Sano et al. 2013).
The aim of this paper is to demonstrate that variations in elemental data associated with terrigenous content in a carbonate-dominated succession can be used to provide a chronostratigraphic correlation in carbonate settings. In order to achieve this goal, two chronostratigraphically well-constrained field sections from a carbonate platform-top setting were analyzed. The work also demonstrates that published approaches using elemental chemostratigraphy in siliciclastic settings, such as definition of isochemical chemozones, which reflect changing provenance or paleoclimate, do not provide meaningful results in the two field sections studied.
Inorganic geochemical data were gathered from two field sections in the Canning Basin, Western Australia (Fig. 1). The sections are both in the Windjana Gorge area (Fig. 1) and contain sequences of mid-late Frasnian age, deposited in a platform-top setting, on a narrow (~5 km) attached platform (Playford et al. 2009, Playton et al. 2016). The narrow shelf resulted in a terrestrial source always in close proximity to the carbonate factory on the platform top, yielding intricately commingled siliciclastic and carbonate lithologies (Fig. 2). The two studied sections, referred to as Windjana north A (WNA) and Windjana north B (WNB), are approximately 1 km apart and are 143 m and 171 m thick, respectively (Figs. 2, 3).
The work presented herein on the WNA and WNB sections is part of the Canning Basin Chronostratigraphy Project (CBCP), a multidisciplinary project integrating biostratigraphy, paleomagnetism, and stable isotope stratigraphy with field logging and sequence stratigraphy (Playton et al. 2016). The goal of CBCP, which includes numerous sections in addition to WNA and WNB, is to develop a chronostratigraphic correlation framework for the Middle to Upper Devonian carbonate system of the Lennard Shelf in Australia (Playton et al. 2016). Playton et al. (2016) demonstrate that the reefal system on the Lennard Shelf represents a supersequence spanning more than 25 Myr of time (second-order sequence of Sarg et al. 1999; after Playford et al. 2009; Playton and Kerans 2015a, 2015b; absolute age after Gradstein et al. 2012). When the two field sections of this paper are placed within the regional chronostratigraphic framework developed by the CBCP, they are shown to contain a supersequence maximum flooding surface (MFS) that separates a supersequence transgressive systems tract (TST) from a supersequence highstand systems tract (HST) (Fig. 10 of Playton et al. 2016; Figs. 2, 3). The two study sections contain portions of only two composite sequences (Fr5 and Fr6) (Fig. 3). The supersequence and component composite sequences are described in detail in Playton et al. (2016), where comparisons with sequences from previous research (George et al. 2009, Playford et al. 2009) are presented.
A physical tie between the two sections was provided by a ground truthing correlation done in the field during the generation of detailed field logs (Fig. 2), and refined stratigraphic correlation between the two sections was achieved using geomagnetic polarity reversals (Hansma et al. 2015, Hillbun et al. 2015, Playton et al. 2016). Regionally, additional stratigraphic data for the succession are provided from carbon isotope curves and conodont biostratigraphy. However, the primary marine isotopic signal that is needed to define chronostratigraphically significant excursions from carbon isotope data is compromised in the platform-top settings due to meteoric diagenetic overprint (Playton et al. 2016). Although conodont biostratigraphy is well established for Upper Devonian sequences in the Canning Basin (Klapper 2007), age-diagnostic Devonian conodonts are most common in slope to basin settings, and therefore platform-top sequences generally lack biostratigraphic control (Roelofs et al. 2015, Playton et al. 2016). Despite the limitations of carbon isotopes and biostratigraphy in platform-top settings, the high-confidence control from the magnetic reversals and ground truthing from the sections in Windjana Gorge (Figs. 2, 3) provide a well-constrained framework against which the elemental chemostratigraphy can be tested.
In the WNA section, the oldest sediments analyzed are a mixed siliciclastic-carbonate sequence deposited on the inner platform. Here, discrete, but discontinuous calcareous sandstone beds are common, separated by beds of mixed wackestone, packstone, and floatstone carbonate facies. These mixed lithologies pass upward into a series of stromatoporoid-dominated boundstones and floatstones deposited on reef-flat depositional environments (Playford et al. 2009). In WNB, a similar vertical change in facies is seen, but reef-flat facies remain interbedded with mixed-lithology inner- and outer-platform sediments, indicating that WNB was located slightly more landward than WNA (Fig. 3) (Playton et al. 2016).
During field logging, hand samples and core plugs were collected for analysis and were accurately placed within the field logs (Fig. 2). In total, 269 samples were analyzed from WNA, and 339 samples were analyzed from WNB. Although sample spacing was to some degree controlled by exposure, an average sample spacing of approximately 50 cm was achieved in each field section (Table 1 in Playton et al. 2016).
Initially, all field samples were cleaned, and parts obviously affected by modern-day surficial weathering were removed. Approximately 10 g aliquots of the remaining sample were then ground to a fine powder in a ball mill. Although a 0.25 g aliquot of powder is used for analysis by inductively coupled plasma instruments, the 10 g homogenized powder sample provides better representation of the formation than 0.25 g of powder. In order to best carry out chemostratigraphic studies, data for a wide array of major and trace elements are required, and instrumentation that can detect and quantify these trace elements at very low abundances is needed for carbonate lithologies. For this study, the elemental data were acquired using inductively coupled plasma-optical emission spectrometry (ICP-OES) and inductively coupled plasma-mass spectrometry (ICP-MS), following a Li-metaborate fusion (Jarvis and Jarvis 1995). This methodology provides data for 10 major element oxides (SiO2, TiO2,Al2O3, Fe2O3, MgO, MnO, CaO, Na2O, K2O, P2O5), 25 trace elements (Ba, Be, Bi, Co, Cr, Cs, Cu, Ga, Hf, Mo, Nb, Ni, Pb, Rb, Sn, Sr, Ta, Tl, Th, U, V, W, Y, Zn, Zr), and 14 rare earth elements (La, Ce, Pr, Nd, Sm, Eu, Gd, Tb, Ho, Dy, Er, Tm, Yb, Lu).
APPLYING CHEMOSTRATIGRAPHIC METHODS TO WNA AND WNB
Published accounts of elemental chemostratigraphy largely adopt a similar approach, where elemental data from lithologically similar intervals are used to define isochemical intervals of sediment termed chemostratigraphic packages (e.g., Ratcliffe et al. 2015 and references therein) or chemozones (e.g., Ramkumar 2015). A similar approach is explored here, and its limitations for this carbonate system study are discussed.
Lithological Normalization and Separation
Publications on siliciclastic chemostratigraphy advocate that different lithologies should be considered separately from one another when defining stratigraphic correlations (Pearce et al. 2005; Ratcliffe et al. 2006, 2015; Hildred et al. 2010). This, the authors argue, negates changes in elemental composition that reflect gross lithological changes, thereby allowing more subtle variations in elemental chemistry that reflect provenance, climate, etc., to be recognized in lithologically similar facies. Furthermore, authors commonly argue for normalization of elements against Al2O3 to minimize the effect of changes in silt and clay contents of lithologies (Van der Weijden 2002; Pearce et al. 2005, 2010; Ratcliffe et al. 2015), although the validity of this approach has recently been questioned (Lowey 2015). These approaches proved problematic within the intricately mixed carbonate and siliciclastic lithologies of this study.
In a carbonate-dominated setting, Al2O3 and SiO2 concentrations are typically linked to terrigenous clay and quartz contents, whereas CaO reflects the amount of carbonate. In such a system, SiO2 and Al2O3 display a positive linear association with one another and negative association to CaO; i.e., as carbonate increases, terrigenous-derived content decreases. Figure 4A shows that while the majority of samples define a positive linear association (trend 1) on a SiO2 vs. Al2O3 cross-plot, two additional trends are noted. Trend 2 is formed by samples with high SiO2 values that show lesser associated increases in Al2O3 than trend 1 samples. Trend 3 is defined by samples with high Al2O3:SiO2 ratios relative to the samples that form trend 1. High SiO2 indicates higher quartz contents, whereas higher Al2O3:SiO2 values indicate higher clay contents. The samples that form trend 3 on Figure 4A (high Al2O3:SiO2) are generally associated with stromatoporoid and microbial boundstones in the reef-flat facies, not, as would be expected, associated with the siliciclastic facies. High Al2O3 values, attributable only to fine-grained siliciclastic material (clay), are more common in the boundstone-associated facies than in the siliciclastic-dominated facies. This association of Al2O3 (clay) and boundstone facies could be due to reef-flat organism’s preferentially binding sediment during their growth and/or sediment infilling of depositional cavities in reefal boundstone (Fig. 5A).
Samples that form trend 2, as expected, are associated with the sandstone beds at the base of WNA. However, there are also samples with high SiO2 and SiO2/Al2O3 values associated with reef-flat facies, where sandstone beds have not been recorded. These high SiO2, low Al2O3 samples in the reef-flat facies are associated with silicification and coarse quartz grains bound within the reefal sediments, both of which were observed in the field (Fig. 5B).
Therefore, while the mineralogical changes implied from elemental data in WNA and WNB can be readily explained geologically, the complex controls on lithologies in this mixed carbonate-siliciclastic setting negate the rationale of lithological sorting and Al2O3–normalization employed by siliciclastic chemostratigraphy studies.
The dolomitization recorded in the WNA and WNB sections adds another level of complexity to the interpretation of whole-rock inorganic geochemical data. Figure 4B and C display Al2O3 vs. CaO and SiO2 vs. CaO cross-plots, respectively. On both binary plots, two negative trends are defined, both implying that as carbonate increases, quartz and clay decrease. As Figure 4D shows, there is a range of carbonates, from limestone with over 50% CaO and MgO <2% to dolomites with MgO >15%. The distributions of SiO2, Al2O3, CaO, and MgO as proxies for quartz, clay, calcite, and dolomite within the sections are displayed in Figure 6.
Definition of Isochemical Chemostratigraphic Packages
Published siliciclastic chemostratigraphic papers define chemostratigraphic packages (e.g., Ratcliffe et al. 2010, 2015) or chemozones (e.g., Ramkumar et al. 2011, Craigie 2015) as the primary correlative features. Both chemostratigraphic packages and chemozones are defined as having distinctive element or element ratio values when compared to the rest of a section. Packages normally have a stepped base and top and therefore represent a discrete sequence of sediments that are “chemostratigraphically” distinctive and can be defined using graphical plots such as binary and ternary diagrams and using multivariate statistical methods such as principal components analysis. On Figure 6, a clear upward increase in MgO values at 57 m above the base of the WNA section shows a stepped change in concentration that can be used for chemostratigraphic package definition. However, the MgO values, as discussed already, are controlled by the amount of dolomitization, a feature that is unlikely to be of regional stratigraphic significance because dolomite bodies are not correlative over short distances in the field. Therefore, as discussed by many chemostratigraphic workers (e.g., Ratcliffe et al. 2010, 2015), if package definition is to be stratigraphically useful, it needs to be based on element ratios that are related to changes in parameters that are linked to stratigraphy.
The approach of defining stratigraphically significant isochemical packages has been tried in WNA and WNB, using elemental ratios interpreted in the literature to be paleoclimate driven (Ga/Rb; Ratcliffe et al. 2010), feldspar content driven (K2O/Rb; Ratcliffe et al. 2006, Wright et al. 2010), and provenance driven (Zr/Cr—Ratcliffe et al. 2007; Zr/TiO2—Pearce et al. 2005, Stüben et al. 2005). The chemical logs are displayed on Figure 7, where it is apparent that the amount of variation between closely spaced samples is typically large when compared to the overall variation in the entire section, resulting in chemical logs that lack systematic variation. Even when a moving average is applied in an attempt to negate small-scale chemical fluctuations, there are no obvious systematic trends in the chemical logs on Figure 7. The types of stepped changes described in many siliciclastic chemostratigraphy papers are not apparent in WNA and WNB, therefore making definition of isochemical chemostratigraphic packages problematic.
CHEMOSTRATIGRAPHIC CORRELATION OF WNA AND WNB
When Zr is plotted as chemical logs for WNA and WNB, cyclical variations are apparent (Fig. 8). Furthermore, the shape of the cycles changes through time within a section. Zr concentrations best display the cyclical variations in the two study intervals of this paper (Fig. 8). Zr is commonly used as a proxy for the heavy mineral zircon in both siliciclastic and carbonate studies (Pearce et al. 2005, Stüben et al. 2005, Ratcliffe et al. 2012, Sano et al. 2013, Craigie 2015). The only source of zircon is a terrigenous one; i.e., it cannot be derived by interactions with seawater. Zircon is also mechanically and chemically stable (Hubert 1962), remaining unaffected by early or late burial diagenesis (Morton and Hallsworth 2007); hence, it is an effective proxy for terrigenous input. Therefore, Zr concentrations in carbonate sediments will reflect the amount of zircon deposited, which in turn will relate to the amount of terrigenous material in the carbonate.
In the oldest parts of the studied intervals, each Zr cycle displays a gradual upward increase to a maximum, followed by a sharp decrease (cycles labeled 1a–6a on Fig. 8), giving a clear sawtooth Zr stacking pattern in the lower parts of the study intervals. Each one of these upward-increasing Zr sequences is approximately 10 to 15 m thick. At 82 m above the base of the WNA section, a maximum in Zr values (7a) is followed by a 10-m-thick sequence in which the Zr values gradually decrease upward (labeled 7b in Fig. 8). This paired association of upward increase (7a–10a) and upward decrease (7b–10b) is continued in the upper parts of the studied intervals, reflecting a marked change in the Zr stacking pattern at 82 m in WNA (Fig. 8).
In WNB, the Zr stacking pattern exhibits a sawtooth pattern of upward gradual increases to a maximum, and then a sharp fall until 50 m above the base of the section. Above 50 m in WNB, the patterns are more symmetrical, with upward-increasing sections followed by upward-decreasing patterns (Fig. 8). The first significant upward-decreasing Zr trend (7a–7b) occurs at 50 m in WNB and 82 m in WNA, allowing this signature to be correlated between the two sections. The change in character in WNA is within a reef-top sequence of boundstones, whereas in WNB, it is within a siliciclastic-carbonate sequence of inner- to outer-platform deposits, suggesting the change in Zr stacking pattern is independent of facies. On Figure 8, the correlation line between 82 m in WNA and 50 m in WNB is immediately below the top of the Fr-R2 Chron (for discussion of paleomagnetic chron nomenclature, see Playton et al. 2016), indicating that the change in Zr stacking patterns is synchronous in the two sections. Figure 8 further demonstrates that above and below this change, maxima and minima in the Zr-stacking patterns match the paleomagnetic, physical, and supersequence MFS correlation. This suggests that the Zr-based stacking pattern correlation is chronostratigraphic between WNA and WNB.
The cycles used for the correlation between WNA and WNB are decimeter-scale features (Fig. 8). However, cyclicity is also apparent on the meter and hundred-meter scales. The values of Zr at each maximum (labeled 1a–7a in WNA) display an overall upward increase, suggesting a cyclicity that is larger than the scale of these two sections on the scale of hundreds of meters. Finer-scale repetitive rhythms of parasequence scale are definable in places of higher sample density (e.g., 6a in WNB on Fig. 8).
While control on Zr concentration is unequivocally the amount of zircon derived from the nearby large landmass, the reason zircon varies systematically and in a time-significant manner is not readily apparent. The multiscaled (meters, decimeters, and hundreds of meters), repetitive rhythmic stacking seen in the Zr chemical logs is reminiscent of variations in sediments controlled by base-level fluctuations, irrespective of the actual variable being analyzed. For example, one can compare the Zr stacking patterns to the sigmoids, sets of sigmoids, and cosets of sigmoids of Pomar and Ward (1994, 1995) and resultant rhythmic variation in magnetic susceptibility described by Davies et al. (2013) in the reef complexes of Mallorca. Numerous authors have used magnetic susceptibility as a proxy for terrestrial input and demonstrated a base-level control (Da Silva and Boulvain 2002, 2006; Racki et al. 2002; Hladil et al. 2003; Da Silva et al. 2009). However, if a base-level control was responsible for the Zr stacking patterns in WNA and WNB, they should be expected to show close correspondence with the carbonate facies cycle stacking patterns defined by Playton et al. (2016). While in some cases the tops of Zr cycles correspond to carbonate cycle tops (e.g., Zr cycles 5a and 6a on Fig. 8), there is no consistent correlation between the two types of cycles. Additionally, in places, Zr maxima correspond to the top of upward-shoaling cycles, whereas elsewhere, they are coincident with the top of upward-deepening cycles (Fig. 8). Therefore, potentially, the Zr cycles were not created solely in response to base-level fluctuations.
Although the individual Zr cycles do not always correspond to carbonate cycles, the change from sawtooth Zr chemical logs to more symmetrical Zr chemical logs occurs in association with the interpreted supersequence MFS (Fig. 8) in WNA and WNB (Playton et al. 2016). One potential explanation for this change in Zr stacking patterns in association with the supersequence MFS is an increase in biohermal/reef-flat facies at the supersequence MFS in the two sections. Biohermal facies are highly productive, and with increased accommodation associated with the MFS, increasing carbonate production in a reef-flat setting would dilute clastic content, assuming relatively constant clastic supply.
In the depositional system studied, where there are clear, well-defined sandstone beds derived from a nearby landmass, it is reasonable to assume that zircon delivery to the shelf was riverine. If this assumption is correct, cycles 1 through 6 would indicate a repeated pattern of gradual increase in silt- to fine-sand-sized terrigenous content of the sediment over approximately 10 m of section, followed by a sharp decrease over about 50 cm of section (the resolution of sampling). Cycles 7 through 10, by contrast, indicate a repeated pattern of gradual increase in terrigenous content, followed by a gradual decrease in the terrigenous content. In this case, cycles 1 through 6 likely represent a prograding sequence, culminating in a maximum regressive surface (MRS), followed by rapid flooding and a MFS almost coincident with the MRS. Such stacking patterns would be inconsistent with the position in a long-term TST, because cycles within longer-term TSTs should have part of the flooding/rise preserved within them.
Another delivery mechanism for terrestrial material into carbonate settings is from windblown detritus. Examples where this is the primary delivery mechanism are from isolated carbonate platforms, such as those described by Davies et al. (2013). This is not the case for this part of the Lennard Shelf. In isolated platform settings, the amount of windblown detritus being delivered to the system is relatively constant and changes slowly in response to large global shifts in climate. In these cases, the terrigenous content of the deposited sediments is still linked to base-level fluctuations, where carbonate productivity and accommodation become the primary control; low carbonate productivity and low accommodation result in high terrigenous content, whereas high productivity and high accommodation dilute the windblown detritus (Da Silva et al. 2012). Assuming this mechanism, the Zr stacking patterns in cycles 1 through 6 would start with high accommodation and reduce to a minimum at the top of a cycle, before a rapid increase in accommodation. Therefore, a windblown delivery mechanism means the transgressive-regressive patterns suggested by the Zr concentrations are again inconsistent with the move toward a supersequence TST, where overall deepening and preservation of both prograding and retrograding parts of cycles would be expected. Furthermore, the rapid fluctuations of the Zr concentrations suggest that long-term climatic fluctuations are unlikely to have been the driving factor, and the coarser quartz fraction is too large for windblown processes.
Reworking of the clastic component, postdelivery, will influence the distribution of sediments on the shelf. The narrow shelf would have been prone to current sweeping and longshore drift processes, and the complex reentrant and promontory paleogeography of the shelf (Playford et al. 2009) would have caused complexity in currents, with resultant highly localized sediment dispersal patterns. A mixture of primary delivery signal and reworked signal in the clastic component potentially explains why, in places, Zr stacking patterns match carbonate cycle stacking patterns, but in other places, they do not.
Siliciclastic detritus is recorded throughout the shelf deposits, and beyond into other depositional settings of the shelf complex, intricately commingled with the carbonates and also forming discrete sandstone beds (Playton et al. 2016). The sandstone beds recorded in the back reef environment are not contiguous on the scale of this study and do not lend themselves to parasequence set interpretation because of their discontinuous character. This suggests that the terrestrial component, in this case, in the form of sandstone beds, was not reacting exclusively to base level. The ubiquitous presence of siliciclastic material in the platform-top setting was due to the constant proximity of the shoreline, which in turn was due to the narrowness of the carbonate platform in this area. This close proximity and constant supply of terrestrial detritus may be the reasons that terrestrial content fluctuations do not follow a classic carbonate-siliciclastic model with reciprocal sedimentation (Wilson 1967, Meissner 1972).
The detailed relationship between siliciclastic distribution and carbonate facies on the Lennard Shelf is outside the scope of this stratigraphic paper, but it warrants further investigation, both on the local scale as seen in the WNA and WNB sections, as well as further afield using other sections in the CBCP.
This paper demonstrates that with paleomagnetic and ground truthing stratigraphic control on stratigraphy, high-resolution chronostratigraphic correlation between the two study sections can be achieved using cyclical changes in Zr concentrations. While no rigorously tested hypothesis for the controls on the Zr cycles can be put forward with the current data sets, it is apparent that the change in shape of cycles is coincident with the supersequence MFS and may therefore be a regionally significant feature. The peaks and troughs, however, likely only afford a local correlation feature.
Published approaches of chemostratigraphic siliciclastic workers in the mixed carbonate-siliciclastic sequences of the WNA and WNB sections do not provide meaningful results in this area. No clear stepped changes in elemental concentrations or element ratio values that relate to changes in provenance or paleoclimate can be identified in the sampled sections. Variable dolomitization prevents the use of trace element data for definition of paleoredox-based changes. Therefore, it is impossible to identify and correlate isochemical intervals; i.e., the chemostratigraphic packages or chemozones used by siliciclastic workers. However, with the stratigraphic constraints afforded by the paleomagnetism and ground truthing correlation, it is demonstrated here that the Zr stacking pattern approach does provide chronostratigraphically meaningful correlations.
The work in this paper is based on two closely spaced sections of limited stratigraphic extent from a platform top in the Canning Basin, an attached carbonate platform. However, the approach described can be applied to any sequence, irrespective of stratigraphic extent or age, depositional setting, or geological basin, including detached carbonate platforms, where airborne dust provides the terrigenous-related elemental signatures. Furthermore, the approach is applicable to subsurface settings where core and cuttings samples are available, thereby potentially providing a stratigraphic tool for the petroleum industry.
We especially thank the Aboriginal tribes of the Bunaba and Gooniyandi (Kuniandi) people, who allowed us to conduct this research on their sacred lands. Thanks go to Paul Montgomery and Peter Cawood for the integrated chronostratigraphic vision, and to Phil Playford for introduction to the outcrop belt. Funding was supplied by the Australian Research Council Linkage Program (grant LP0883812), ARC-QEII Grant Program, ARC-DORA–3 Grant Program, Minerals Research Institute of Western Australia (MERIWA), Western Australian Energy Research Alliance (WAERA), Commonwealth Scientific and Industrial Research Organization (CSIRO), Buru, Chevron Australian Business Unit, Chevron Energy Technology Company, the University of Greenwich, and Chemostrat, Ltd. Field support and safety were provided by Wundargoodie Aboriginal Safaris (Colin and Maria Morgan and family and crew), the Geological Survey of Western Australia, Chevron Australian Business Unit, and Steve Meyer, Sean O’Connell, and Bill Robinson of Chevron. Thanks go to Windjana Gorge National Park, Napier Downs, the Mimbi Community, Mount Pierre Station, Fossil Downs Station, Brooking Downs Station, the Pillara Mine, and the Cadjebut Mine for field area access and resources. Thanks also go to R. Addenbrooke, H. Allen, A. Duffy, G. Beacher, M. Diamond, M. Ducea, K. Grice, J. Hansma, K. Hillbun, T. Holland, J. Hsieh, D. Katz, J. Klemm, L. Lanci, K. Liebe, E. Maslen, L. McEvoy, F. Pardini, S. Pisarevsky, T. Raub, B. Roelofs, S. Shoepfer, U. Singh, S. Slotznick, S. Tulipani, M. Thorp, K. Trinajstic, T. Tobin, A. Vonk, F. Wellmann, P. Ward, and K. Williford for field assistance and project-related contributions beyond the scope of this paper. Roger Hocking and Peter Haines publish with the permission of the executive director of the Geological Survey of Western Australia. The Chemostrat authors would like to thank Chemostrat for allowing them time to publish this work. The authors are also grateful to the two referees, both of whom made invaluable suggestions that improved the publication.