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Appendix BNotes linked to Figure 13 Within the Perth Basin (Playford et al., 1976), marine Sakmarian–Artinskian deposits are confined to the northern parts of the basin, and crop out only in the Irwin Sub-basin (also called Irwin Terrace) which is a continuation of a narrowly elongate interior rift that extends from the Southern Carnarvon Basin (viz. from north to south, the Merlinleigh, Byro and Coolcalalaya Sub-basins; Mory and Iasky, 1996; Iasky et al., 1998; Mory et al., 1998a; Mory and Haig, 2011). The Irwin Sub-basin is separated from the Dandaragan Trough (the northern part of which, in subsurface, contains a comparable Sakmarian–Artinskian succession) by a major fault and a basement high. Sakmarian–Artinskian marine deposits are confined to interior rift (half-graben) basins along the eastern side of the Southern Carnarvon Basin (Hocking et al., 1987; Iasky et al., 1998; Mory et al., 1998a; Mory and Haig, 2011). These have been designated, from north to south, the Merlinleigh, Byro and Coolcalalaya Sub-basins (the latter has also been included in the Perth Basin). To the west of these sub-basins lies the Gascoyne Platform that formed a topographic high during the Permian (Mory et al., 1998b; Iasky et al., 2003). A greater marine influence toward the north is apparent in a Lower Permian transect from the Sue Coal Measures of the southern Perth Basin to the fully marine succession in the northern Merlinleigh Basin (Playford et al., 1976; Hocking et al., 1987). The Nangetty Formation was established by Clarke et al. (1951) who characterised it as “tillites, glacial shales, fluvio?glacial sandstones, locally with calcareous grits and sandstones showing ‘Fontainebleau’ structure, underlain by further glacial shales and basal conglomeratic grits” with estimated thickness of about 240 m. They placed the boundary between the Nangetty Formation and the overlying Holmwood Shale at the “transition from glacial shales (with angular fragments and occasional boulders), into the dark grey shales”. Playford et. al. (1976) redescribed the formation and noted a thickness of more than 1,500 m adjacent the Urella Fault. Eyles et al. (2006) described facies associations interpreted mainly as deposits transported from meltwater to form fan deltas at the margins of a fiord?like basin. Plant microfossils and foraminifera are the only fossils known from the formation (Playford et al., 1976; Skwarko, 1993). According to Mory et al. (2008, fig. 2), the G. maculosa, S. ybertii, D. birkheadensis, D. tentuistriatus, Stage 2, and P. confluens Zones (in ascending stratigraphic record) are represented in the Nangetty Formation. No age?indicative ammonoids, conodonts, or fusulinids are known from the formation and the age of the boundary with the Holmwood Shale has not been established with any precision.The Lyons Group, described in detail by Condon (1967) and Hocking et al. (1987) includes a succession of mudstone, sandstone and laterally extensive sheet?like diamictite deposits that suggest glacial influence. Thickness of the group in some areas exceeds 1500 m but is variable. Few fossil localities have been identified scattered through the succession; these contain bryozoans, bivalves (including Eurydesma), gastropods, scaphopods, conularids, brachiopods, crinoid debris, foraminifera, “corals”, “worm trails”, and wood fragments (Dickins and Thomas 1956, 1959; Condon, 1967; Skwarko 1993). The palynomorphs belong to “Stage 2” and the overlying P. confluens Zone (Mory and Backhouse, 1997; Backhouse, 1998). No age?indicative ammonoids, conodonts or fusulinids are known from the Group and the age of the boundary between the Lyons Group and overlying formations has not been established with any precision. Although all the main studies on the Nangetty Formation and Lyons Group identify significant glacial influence, there is debate about whether deposition was directly from melting glaciers (e.g. Condon, 1967) or from material transported in meltwaters to the depositional site (Eyles et al., 2006). The disappearance of diamictites and dropstones is considered here to represent a significant climatostratigraphic horizon. Eyles et al. (2006) reported rare “ice?rafted boulders” that lack striations in the Holmwood Shale above this horizon. These were not reported in Clarke et al. (1951) or Playford et al. (1976) and have not been seen by Haig (this study) in the Irwin River successions. Large dark?grey calcareous mudstone nodules, some of which contain bryozoa, brachiopoda, ammonoids, echinoderm debris, and foraminifera, are present at various levels in the Holmwood Shale. The Holmwood Shale was originally described by Clarke et al. (1951) and revised by Playford et al. (1976) who designated a type section and, following Johnson et al. (1954) included the “Fossil Cliff Formation” of Clarke et al. (1951) as a member within the formation. Palaeobathymetric trends through most of the Holmwood Shale have not been analysed. The lowest muddy sandstone unit in the High Cliff Sandstone contains large-scale low-angle clinoforms that are truncated by erosion at the top and downlap onto the uppermost mudstone unit of the Holmwood Shale. These suggest a small delta prograding from the northwest with water depth of the sand-mud boundary at about 2.5 m. A very shallow wave-base and consequent sand-mud transition is consistent with an interior-sea setting. The lowest ammonoid found in the Holmwood Shale is Juresanites jacksoni from the Beckett Member of Playford et al. (1976). Teichert and Glenister (1952), Glenister and Furnish (1961), Glenister et al. (1973), Glenister et al. (1993), and Leonova (1998, 2011) have discussed the generic attribution of this species (including the synonym J. campbelli, also recorded from the Holmwood Shale). Glenister et al. (1993) recorded the Beckett Member as about 370 m below the top of the Holmwood Shale. Playford et al. (1976) measured the Beckett Member at 168 m above the base of the Holmwood Shale. Leonova (2011) placed J. jacksoni with J. somoholensis (Timor), J.? maximovae (N?W Russia), and J. kazakhorum (Urals) within the Sakmarian. This assemblage of Juresanites and Uraloceras is from higher in the Holmwood Shale than 10. It is known from a level about 46 m above the Beckett Member (10) and 326 m below the top of the Holmwood Shale, at about 28.9700°S, 115.5139°E (Glenister and Furnish 1961). It is also present in the Woolaga Limestone Member of Playford (1959), a 1 m thick nodular muddy “limestone” about 60 m below the top of the Holmwood Shale at about 29.2056°S, 115.6583°E. Glenister et al. (1993) considered U. irwinense as an advanced form of Svetlanoceras transitional to Uraloceras with closest similarities to Paragastrioceras ultaganense from the Sterlitamakian of the southern Urals. Leonova (1998, 2011) regarded the species as closer to Uraloceras than Svetlanoceras and considered that the age was Sakmarian. The small Juresanites in the assemblage was originally named a new species, Metalegoceras campbelli, but considered synonymous with J. jacksoni by Glenister et al. (1993) and later authors. Glenister et al. (1993) suggested that J. jacksoni has it closest affinities to Tastubian (Early Sakmarian) forms of the genus. Juresanites does not range higher than the Sakmarian (Boiko, et al., 2008). This record of Juresanites in the Holmwood Shale is from near the junction of the North and South branches of the Irwin River (Glenister et al., 1993). They considered it to be the highest record of the genus in the formation.According to Condon (1967) the Carrandibby Formation “consists of shale, calcilutite, and sandstone unconformable on the Lyons Group and conformably overlain by the Callytharra Formation". He recorded about 59 m in the type section that lies on the basin margin above an apparent veneer of Lyons Group overlying Precambrian basement. Foraminifera, bryozoa, crinoidea, blastoidea, brachiopoda, bivalves, gastropods have been recorded from the formation (Skwarko, 1993; Dixon and Haig, 2004). Dixon and Haig (2004) found that a conformable facies transition is present from the upper part of the type section of Carrandibby Formation into the overlying type section of the Callytharra Formation. No age-diagnostic ammonoids, conodonts, or fusulinids have been found in the Carrandibby Formation. To the north of present-day 24°S, sparsely fossiliferous sandy mudstone, containing no dropstones, is present between the highest diamictite and the first skeletal packstone unit. This may be equivalent to the Carrandibby Formation further south. In the Dead Man's Gully section at 23.8925°S, 114.9638°E (Mory and Haig, 2011) the sandy mudstone unit is about 10 m thick. Palaeobathymetric trends in units below the Callytharra Formation have not been analysed. The large thick-shelled bivalve Eurydesma is conspicuous in the type section of the Carrandibby Formation and considered to be characteristic of cold water (Dickins, 1957; Dickins and Skwarko, 1993). The base of the lowest skeletal packstone bed in the lowest parasequence of a set defines the base of the Callytharra Formation in the Southern Carnarvon Basin (see parasequence pattern, caused by cycles of friable mudstone to indurated packstone, apparent on 2008 Goggle Earth image at, for example, 23.8935°S, 114.9627°E and along strike from this). The cyclic pattern is not as well expressed in the northern Perth Basin where a reduced succession containing carbonate beds is present. The base of the Fossil Cliff Member is defined by the lowest muddy packstone in the lower set of muddy packstone/shelly mudstone beds (see log in Mory et al., 2005, fig. 42). This level lies near the boundary between the P. confluens and P. pseudoreticulata spore-pollen zones in both the Southern Carnarvon and the northern Perth Basins (Foster et al., 1985; Mory and Backhouse, 1997). Condon (1967) discussed the history of nomenclature of the Callytharra Formation and redefined the formation as “fossiliferous hard and friable sandy and silty calcarenite and calcilutite, siltstone, and quartzwacke conformably (?disconformably) overlying the Carrandibby Formation or unconformably overlying formations of the Lyons Groups and Precambrian schist and overlain unconformably by formations of the Wooramel Group". Mory and Backhouse (1997) placed the Jimba Jimba Calcarenite in the upper part of the Callytharra Formation. Dixon and Haig (2004) remeasured and redescribed the type section (146 m thick), including the biofacies succession and found that this includes probably only the lower part of the section known north of 24°S. The Callytharra Formation contains a diverse assemblage of macrofossils including tabulate and solitary rugose corals, bryozoans, brachiopods, bivalves, ammonoids, nautiloids, gastropods, conulariids, blastoids, crinoids, plants, annelids (Spirorbis) (Skwarko, 1993). Playford et al. (1976) discussed the history of nomenclature of the Fossil Cliff Member and the lenticular nature of the limestone beds of apparently limited extent. Mory et al. (2005, fig. 42) presented a log and facies interpretation of the type section. The Member contains a diverse macrofossil assemblage including tabulate and solitary rugose corals, bryozoans, brachiopods, bivalves, ammonoids, nautiloids, gastropods, trilobites, and crinoids (Skwarko, 1993). A change in palaeobathymetric trend from progradation to retrogradation is represented at 4.5 m and 11.8 m above the base of the Fossil Cliff Member in the type section (see Mory et al., 2005, fig. 42). In terms of "secondary" depositional cycles, the change at 11.8 m, at the top of the last "packstone" unit in the succession, is taken as more significant for regional correlation. This maximum flooding event (the change from a retrogradational to a progradational bathymetric trend) is represented at about 13 m above the base of the Fossil Cliff Member in its type section (Mory et al., 2005, fig. 42). A change in palaeobathymetric trend from progradation to retrogradation is represented at about 5 m above base of the Callytharra Formation in the Dead Man's Gully section (Fig. 16 of the present study). This level is clearly seen at 23.8929°S, 114.9620°E (Google Earth Image 2008) and along strike from this point. This maximum flooding level is represented at about 30–40 m above base of the Callytharra Formation in the Dead Man's Gully section (Fig. 16 of the present study). This can be seen at about 23.8945°S, 114.9606°E (Google Earth Image 2008) and along strike from this point. Archbold and Hogeboom (2000) established Cimmeriella as a new brachiopod genus with C. foordi as type species. The species is present in the Fossil Cliff Member and in the lower part of the Callytharra Formation (Archbold, 1983). In the Dead Man's Gully section (Fig. 16 of the present study) it is present only in the lower 5 m of section (Mory and Haig, 2011); whereas in the type section of the Callytharra Formation (Fig. 18 of the present study) it is present throughout the 0–60 m interval containing skeletal packstones. The ammonoid Metalegoceras kayi, based on the one specimen found at Fossil Cliff, has a primitive suture (Glenister et al. 1993). According to Glenister et al. (1993) the range of the genus is firmly established as Lower Sakmarian (Tastubian) through Upper Artinskian (Baigendzhinian) and known species with the closest overall affinities to M. kayi are M. distale and M. noinskyi indicative of the Sakmarian. Boiko et al. (2008) placed M kayi in the subgenus Metalegoceras. Leonova (2011) also regarded M. kayi as Sakmarian. The last occurrence of P. confluens and the concomitant first appearance of P. pseudoreticulata in the spore-pollen succession in Western Australian basins provides a significant palynostratigraphic level for correlation (Mory and Backhouse, 1997; Backhouse 1998). This level lies close to the Callytharra Formation – Lyons Group boundary in the Southern Carnarvon Basin. Uraloceras irwinensis (see comment for 11) was found in the lowest fossiliferous member of the Callytharra Formation at about 24.8723°S, 115.5235°E (Glenister et al., 1990).?Mescalites sp. The taxonomic assignment of this gonioloboceratid (ammonoid) is uncertain (Glenister et al., 1993). It was found in the Callytharra Formation at the same locality as U. irwinensis (27). One specimen identified as Metalegoceras n. sp. by Glenister and Furnish (1961) is known from the base of the Callytharra Formation at about 24.5230°S, 115.3056°E. It differs from M. australe (found in the Timor Bitauni fauna and in the Nura Nura Member of the Poole Sandstone, Canning Basin) by possessing a distinctly arcuate apex on the second lateral lobe but was placed in the upper Sakmarian (Sterlitamakian) (Glenister et al., 1993). Boiko et al. (2008) referred the species to Parametalegoceras sp. with an age of late Sakmarian. This occurrence of Metalegoceras sp. is in the Dead Man's Gully section in the shale-dominated interval around the maximum flooding event (23). The identification was by Tatyana Leonova and the specimens are now in her collection (Mory and Haig, 2011). Small immature morphotypes identifed as Pseudoshistoceras? spp. by Tatyana Leonova (specimens in her collections) are from the same level as 30.This "2nd-order" change from progradation to retrogradation is at around 75 m in the Dead Man's Gully section (Figs. 14, 16). Some beds of quartz sandstone and quartz-rich skeletal limestone are present in the prodgradational part of the sequence from 55–75 m. This interval is correlated with the Winnamea Sandstone (33), Ballythanna Sandstone (34) and part of the High Cliff Sandstone (39) to the south. Mory and Backhouse (1997) established the Winnamea Sandstone as a Member within the Callytharra Formation. It consists mainly of massive sandstone. An interval (11–12.5 m above the base of the Member) in one part of the type area contains well-developed tabular cross-beds that suggest a palaeo-currents flowing toward the southeast (Matthew Dixon, unpublished data). The Ballythanna Sandstone Member of the Callytharra Formation was established by Mory (1996) for the interval 65–298 m in GSWA Ballythanna 1 (at 26.0633°S, 115°6741°E). This maximum flooding event is represented in a shale unit between 75–78 m in the Dead Man's Gully section (Fig. 16 of the present study). The Jimba Jimba Calcarenite was established as a formation between the Moogooloo Sandstone (of the Wooramel Group; see 41) and the Billidee Formation (see Condon, 1967). Based on subsurface information and regional palynostratigraphy, it was placed as an upper member of the Callytharra Formation by Mory and Backhouse (1997). A log of the type section is presented in Fig. 17 of the present study. ‘Propinococeras’ sp. is the only ammonoid recorded from the Jimba Jimba Calcarenite and Skwarko (1993) questioned whether it was Bamyaniceras australe (see 58). Nicoll and Metcalfe (1998) described the conodonts Hindeodus sp. (as H. sp. 1) and Vjalovognathus australis (n. sp.) from the Callytharra Formation (including the type section of the Jimba Jimba Calcarenite). All localities listed by Nicoll and Metcalfe (1998) seem to correspond to levels above the maximum flooding interval 23. Vjalovognathus australis was differentiated from V. shindyensis (Kozur) by the denticles of the Pa elements of V. australis being "essentially round with a narrow groove on the anterior margin of some denticles" compared to the "laterally expanded" denticles with a broader groove in V. shindyensis. They described the species also from the "Maubisse Formation" in West Timor, and regarded it as the oldest known representative of the genus. They regarded the age as late Sakmarian to early Artinskian age ("Mesogondolella bisselli–Sweetognathus inornatus Zone") on the basis of its association with M. bisselli in West Timor. Clarke et al. (1951) and Playford et al. (1976) described the High Cliff Sandstone. Mory et al. (2005, fig. 43) presented a log and facies interpretation of the formation. Palynostratigraphic correlation suggests that it is equivalent to the Ballythanna and Winnamea Sandstone members of the Callytharra Formation (Mory and Backhouse, 1997, fig. 3). The boundary between the Callytharra Formation and the Wooramel Group is a logical conformable facies transition in the progradational part of a sequence: from skeletal packstone to shelly quartz sandstone to fine to coarse-grained quartz sandstone. The boundary is placed at the top of the uppermost skeletal packstone. The Wooramel Group includes the Cordalia Sandstone, mainly composed of thin- to medium-bedded fine-grained quartz sandstone, overlain by the Moogooloo Sandstone mainly composed of medium- to thick-bedded coarse-grained quartz sandstone (Condon, 1967; Hocking et al., 1987). Pseudoshistoceras simile is an advanced metalegoceratid (Glenister et al., 1993; Boiko et al., 2008). Boiko et al. (2008) suggested that Pseudoschistoceras evolved from Metalegoceras during the mid Artinskian. Leonova (2011) placed the Western Australian records of P. simile within the Baigendzhinian Substage of the Late Artinskian below the Kungurian. The Irwin River Coal Measures were described by Clarke et al. (1951); Playford et al. (1976), and McLoughlin (1993). This major marine flooding event is represented in the Perth Basin by the base of the Carynginia Formation. In the Southern Carnarvon Basin evidence for the event lies in the change from very thick-bedded very coarse-grained pebbly sandstone beds to thin- to medium-bedded finer grained quartz sandstone with some units of Skolithus-burrowed "pipe rock" (see Mory and Haig, 2011, fig. 38). This level is within a section mapped as the upper part of the Moogooloo Sandstone.The Billidee Formation was described by Condon (1967) and Hocking et al. (1987). This "2nd-order" maximum flooding event within the Billidee Formation is represented in the thickest shale unit within the formation (at locality 12 on Fig. 38 of Mory and Haig, 2011). The Carynginia Formation was described by Clarke et al. (1951) and Playford et al. (1976). Scattered dropstones are present in the lower Carynginia Formation (see Fig. 47e of Mory et al., 2005), and in the Billidee and lower Coyrie Formations (Hocking et al., 1987). The base of the shelly sandstone mapped at the top of the Billidee Formation by Condon (1967) represents the start of retrogradation (marine trangression) in the depositional cycle that includes the overlying Coryie Formation and Mallens Sandstone. This ammonoid comes from the shelly sandstone near the top of Condon's (1967) Billidee Formation. Neocrimites first appears in the Baigendzhinian Substage of the Upper Artinskian according to Glenister et al. (1993) who suggested that the occurrence Neocrimites sp. was probably at the lower limit of the generic range. Condon (1967) and Hocking et al. (1987) described the Coryie Formation. In the depositional cycle that includes the uppermost Billidee Formation, Coryie Formation and Mallens Sandstone, maximum marine flooding is represented within shale of the Coryie Formation. Glenister and Furnish (1961) noted the similarity of Neocrimites sp. to N. fredericksi. Leonova (2011) proposed a “Neocrimites fredericksi?Medlicottia orbignyana Zone for the Upper Artinskian Substage and showed in the 2002 Lower Permian zonation of the Urals by Chuvashov and others that N. fredericksi occurs in the upper part of the Sarginskian (late Artinskian) below the Saraninskian (Kungurian) and below the level of Neostreptognathodus pnevi. Skwarko (1993) lists “?Bamyaniceras australe” (see 59) in the species list from the Coyrie Formation, but Glenister et al. (1993) only described “Bamyaniceras sp. nov.” = Propinacoceras n. sp. Glenister & Furnish 1961” from this formation (in Appendix to Skwarko, 1993) and suggested a Late Artinskian (Baigendzhinian) age. This species also is present in the Mallens Sandstone. Condon (1967) and Hocking et al. (1987) described the Mallens Sandstone.Condon (1967) and Hocking et al. (1987) described the Bulgadoo Shale. The change from a progradational trend to a retrogradation trend in the marine deposition corresponds to the change from sandstone of the Mallens Sandstone to shale of the Bulgadoo Shale (see logs presented by Hocking et al. 1987).Maximum marine flooding of the "secondary" depositional cycle including the Bulgadoo Shale to Cundlego Formation and of the broader "primary" Artinskian to Roadian depositional cycle in the basin lies in the Bulgadoo Shale (see Mory and Haig, 2011, p. 36–37). Glenister et al. (1993) noted that the ammonoid Bamyaniceras australe belongs to the group of B. simile from the Timor Bitauni fauna and also recognized similarities with B. knighti from the Artinskian (Leonardian = Baigendzhinian) of west Texas. Leonova (2011) placed the records of B. australe in the lower part of the Byro Group within the Baigendzhinian Substage of the Late Artinskian below the Kungurian. The upper portion of the Byro Group also contains Bamyaniceras australe, but with Paragastrioceras wandageense, Pseudoschistoceras gigas, and P. iranense indicative of the Kungurian according to Leonova (2011). Condon (1967) and Hocking et al. (1987) described and presented logs of the Cundlego Formation. Archbold and Shi (1995) noted a "small fauna" of brachiopods including "Tethyan elements" in the Bulgadoo Shale followed by an influx of “warm?water” brachiopods in the Cundlego Formation. This major marine flooding level is at the contact between the Cundlego Formation and Quinnanie Shale (see Haig, 2003, for a description of cycles within the type section of the Quinnanie Shale). The Quinnanie Shale and overlying Wandagee Formation (see Condon, 1967; Hocking et al., 1987) form part of a "secondary" depositional cycle within the "primary" Artinskian-Roadian cycle. The oldest post-glacial "primary" depositional cycle includes the succession from Holmwood Shale to Irwin River Coal Measures in the northern Perth Basin and from the Callytharra Formation to Wooramel Group in the Southern Carnarvon Basin and spans the Sakmarian and lower Artinskian. Maximum flooding in this "primary" cycle is represented at 23. The Byro Group to Kennedy Group "primary" depositional cycle includes the succession from the Billidee Formation to the uppermost formation of the Kennedy Group and spans the upper Artinskian to Roadian. Maximum flooding in this "primary" cycle is represented at 58. Cold conditions are suggested by diamictites and dropstones. Warm?temperate conditions are suggested by the presence of Tubiphytes (as far south as the southern part of the Southern Carnarvon Basin) and foraminifera with non-complex chamber arrangements belonging to the Order Fusulinida (endothryaceans, tetrataxaceans, pseudoammodiscids) (see text of present study). According to Archbold and Shi (1995), the brachiopods include some genera with Tethyan affinities. Cold conditions are suggested by the dropstones (48). The lowest part of Byro Group, including the Billidee Formation to Mallens Sandstone, contains "cold-water" brachiopods (Archbold and Shi, 1995). The Bulgadoo Shale in the lower part of the Bulgadoo-Cundlego depositional cycle, contains some brachiopod genera with Tethyan affinities (Archbold and Shi, 1995). The influx of Tethyan brachiopods (61) suggests "warm-water" conditions. The Sakmarian determination is based on information given for 10-12, 25, 27-29.The Artinskian is based on a change in the ammonoid assemblage with probable Pseudoshistoceras (31) appearing in the second "secondary" depositional cycle (from 22 to 32) and being present in higher cycles. The presence of Neocrimites sp. with similarities to N. fredericksi (53) in cycle 49 to 57 suggests that this interval belongs to the upper Artinskian. It is uncertain whether the Bulgadoo–Cundlego cycle is Artinskian or Kungurian. ReferencesArchbold, N.W., 1983. Studies on Western Australia Permian brachiopods: 3. The Family Linoproductidae Stehli, 1954. Proceedings of the Royal Society of Victoria 95, 237–254.Archbold, N.W., Hogeboom, T., 2000. Subsurface Brachiopoda from borehole cores through the Early Permian sequence of the Carnarvon Basin, Western Australia: correlations with palynological biostratigraphy. Proceedings of the Royal Society of Victoria 112, 93-109. Archbold, N.W., Shi, G.R., 1995. 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