Supplementary paper

General Comments
	The late Paleozoic stratigraphy from eastern Australia is plotted versus the Gradstein et al. (2004) Permian timescale and the Menning et al. (1999) Carboniferous timescale.  The Menning et al. (1999) Carboniferous timescale is the most appropriate timescale for use in Eastern Australia because biostratigraphic data are referenced to European stages.  Events that define the international Carboniferous timescale of Gradstein et al. (2004) are not recognizable in eastern Australia.  Therefore, direct use of the international timescale would be difficult.  As a result, the Carboniferous time-space framework published herein was constructed relative the Menning et al. (1999) timescale, with stages from the international time scale fit to the Menning et al. (1999) timescale and plotted as well, according to published conversions by Heckel & Geoffrey (2006).  Two modifications were made to the Menning et al. (1999) Carboniferous timescale in light of subsequent published scientific data.  The age of the Devonian-Carboniferous boundary was moved to 360.7 Ma, as dated radiometrically by Trapp et al. (2004) from the Hasselbachtal section in Germany.  Additionally, the Visean-Tournaisian Boundary was moved from 342.1 to 345.5 Ma.  The date on the Visean-Tournaisian Boundary in Menning et al. (1999) is based on a radiometric date on the Curra Keith Tongue volcanic member from New South Wales, eastern Australia, published originally in Roberts et al. (1995b).  The date of 342.1 +/- 3.2 Ma was obtained using the SL13 standard, which has since been shown to be a heterogenous standard, and is best corrected to the current TEMORA 1 standard by adding 1% to the original SL13 age, yielding a corrected age of 345.5 Ma for the Curra Keith Tongue and the Visean-Tournaisian boundary (Black et al. 2003).
Eastern Australian published brachiopod, conodont, and palynological zones were plotted relative to the Gradstein et al. (2004) Permian timescale and the Menning et al. (1999) Carboniferous timescale.  Carboniferous brachiopod and conodont biozones were taken from Roberts et al. (1993b), which were updated by Roberts (unpubl. data).  Permian brachiopod and palynological (APP) zones were taken from Briggs (1998).  Late Carboniferous and early Permian palynological zones of Jones & Truswell (1992) were also plotted.    
	A decade-long campaign of U-Pb sensitive high resolution ion microprobe analysis (SHRIMP) dating of Carboniferous and Permian volcanic members throughout eastern Australia has resulted in an improved understanding of the regional stratigraphy and correlation between eastern Australian biostratigraphic zones are the international timescale.  Dozens of radiometric dates from Carboniferous and Permian units across eastern Australia offer a unique opportunity to construct a detailed stratigraphic framework in order to constrain the timing and nature of late Paleozoic glacial deposits.  During the period of dating in the 1990s, U-Pb SHRIMP dating using the SL13 and, later, AS3 standards was the radiometric dating method of choice.  More recent investigation of the method has revealed that the SL13 standard was heterogenous and the SHRIMP I instrument had a low measurement precision compared to the newer instruments (Black et al. 2003).  Additionally, some dates were performed with SL13 and others with the AS3 standard.  At face value, dates using different standards cannot be compared.  
The current preferred standard for U-Pb SHRIMP dating is TEMORA 1.  Black et al. (2003; Claoue-Long pers. comm.) assessed the quality of various current standards, including SL13, AS3, and TEMORA 1, by comparing them to their Isotope Dilution and Thermo-Ionisation Mass Spectrometry (ID-TIMS) age and relative to one another.  The resulting age using the SL13 standard is generally younger than the ages derived from the other standards, and the AS3 weighted mean SHRIMP age is ~1.0 % younger than its IDTIMS age at a 99.9% confidence level (Black et al. 2003).  Results indicate that AS3-based ages are reliably 1% older compared with those derived from TEMORA 1, and SL13 ages are ~1% younger than those based on the TEMORA 1 standard (Black et al. 2003).  
In order to construct an eastern Australia-wide stratigraphic framework, the conversion factor was applied to both SL13 dates (+1%) and AS3 dates (-1%) in order to compare dates from widely-spaced regions in reference to the current TEMORA 1 standard.  Admittedly, the solution is less desirable than re-dating the entire succession using the current TEMORA 1 standard or ID-TIMS methodology.  Early drafts of the eastern Australian late Paleozoic time-space framework published herein were constructed using the original published radiometric dates, without applying a correction to the TEMORA 1 standard.  The framework was plagued with competing stratigraphic schemes and dates that disobeyed the stratigraphic order of units and/or the biostratigraphic data available.  Converting the SL13 and AS3 dates to the TEMORA 1 standard using the conversion factor of Black et al. (2003) resulted in remarkable resolution of stratigraphic inconsistencies.  Additionally, the biostratigraphic and radiometric data were reconciled.  To the authors’ knowledge, applying this 1% conversion to SL13 and AS3 dates is the best method available to maximize the current radiometric dataset, short of replicating the dataset.                          
	During construction of the stratigraphic framework, biostratigraphic data were used as the primary age constraint on each unit.  In most cases, available biostratigraphic data agreed with the converted SHRIMP ages.  However, in some regions of eastern Australia (Myall and Hastings Blocks), radiometric ages were consistently older than those indicated by biostratigraphic data.  In these areas, biostratigraphic data were used as the primary constraint on the age of the formations and SHRIMP ages were left uncorrected.
	Recognition of glacial facies is based primarily on the authors’ field observations and documentation.  In a few cases, time did not permit a full field examination of formations that have been reported to contain glacial facies.  In those cases, the literature source of documented glacial facies is cited.  Representative stratigraphic sections showing the distribution of glacial and nonglacial strata in individual outcrop areas are presented in Figure 1A-E.

Cooper Basin

Subsurface

Merrimelia Formation, Tirrawarra Sandstone, Patchawarra Sandstone, Murteree Shale, Epsilon Formation, Roseneath Shale, Daralingi Formation, Toolachee Formation & Nappamerri Group
The Cooper Basin stratigraphy was taken from Apak et al. (1997).  This stratigraphy is based on the palynological zonation of Price et al. (1985) following from Evans (1967).  The base of the Merrimelia Formation is constrained to the base of APP1.2 palynological zone.  The top of the formation ranges from about halfway up the APP1.2 zone to the early portion of the APP2.1 zone.  The base of the Tirrawarra Sandstone is similarly diachronous, with the top of the formation constrained to the basal portion of the APP2.1 zone.  The late Sakmarian through late Artinskian Patchawarra Sandstone occupies most of the APP2.1 zone through to the basal portion of the APP3.2 zone.  The late Artinskian to early Kungurian Murteree Shale spans the remainder of the APP3.2 zone, while the mid-Kungurian Epsilon Formation is constrained to the APP3.3 zone.  The overlying Roseneath Shale is latest Kungurian in age, based on its restriction to the APP4.1 palynological zone.  The Roadian Darlingi Formation directly overlies the Roseneath Shale and occupies the APP4.2 zone.  The mid-Wordian through mid-Changhsingian Toolachee Formation sits uncomformably the Daralingi Formation and is restricted to the long-lived APP5 palynological zone.  The overlying Nappamerri Group is thought to occupy the remainder of the Permian, continuing into the Triassic (Apak et al. 1997).   

Galilee Basin

Northern Galilee Basin

Drummond Basin SUCCESSION & Joe Joe Group
Palynological study of the Drummond Basin succession reveals a late Devonian to Asbian age (Playford 1977; Playford 1978; Jones & Truswell 1992).  The overlying Joe Joe Group is not identified in the literature from this region.  However, field examination during 2004 revealed the presence of facies from the Joe Joe Group underlying the Boonderoo Beds and overlying the early Paleozoic basement.  The age of the Joe Joe Group is based correlation with the eastern margin of the Galilee Basin, where it is well constrained by palynological data (Jones & Truswell 1992).  Because palynostratigraphic data from the overlying Boonderoo Beds constrain the age of the top of the Joe Joe Group, the Joe Joe Group spans biozones A-D in the northern Galilee Basin (Jones & Truswell 1992).  

Boonderoo Beds & Reids Dome Beds
The Boonderoo Beds are restricted to Australian Permian Palynological zone AP1.22 (Norvick 1974; McKellar 1977), updated to the current palynological zonation scheme (Price et al. 1985; Briggs 1998).  The glacial interval identified within the Boonderoo Beds spans the middle-third of the formation (Jones 2003).  Assuming a linear sedimentation rate, Jones (2003) calculated that the glacial interval spans the middle third of zone APP1.22, placing the Boonderoo Beds glacial interval in the early Sakmarian according to the Gradstein et al. (2004) timescale.  The mid-Tastubian through mid-Aktastinian (mid-Sakmarian through early Artinskian) age of the Reids Dome Beds is taken from palynological data published by Jones & Truswell (1992).  In this scheme, the formation spans palynological zones APP2.1 (formerly base of stage 3a) through the basal portion of APP3.1 (formerly basal portion of lower stage 4).  The assigned age of the top of the formation is in agreement with the subsequent biostratigraphic schemes published by Draper et al. (1990) and Briggs (1998).

Betts Creek Beds  
Jones & Truswell (1992) show the mid-Wordian to mid-Changhsingian Betts Creek Beds to be correlative with the Colinlea Sandstone through Bandanna Formation in the eastern margin of the Galilee Basin, based on palynostratigraphic data.  An interval of strata from within the Betts Creek Beds has been observed in the field to contain sedimentary structures, textures, and fabrics consistent with glacially-influenced deposition.  The mid-Wordian (late Povolzhian) age of this interval of glacially-influenced strata has been constrained via lithostratigraphic correlation to the Freitag Formation in the Denison Trough of the Bowen Basin.  

Eastern Margin of Galilee Basin

Drummond Basin Sequence, Joe Joe Group & Reids Dome Beds
	The age of the Drummond Basin succession is based on palynostratigraphic data (Playford 1977; Playford 1978; Jones & Truswell 1992).  Palynological study of the Joe Joe Group places the unit in biozones A-E in the eastern margin of the Galilee Basin (Jones & Truswell 1992).  The Lake Galilee Sandstone is contained within the Joe Joe Group and contains glacially-influenced strata.  The age of the Lake Galilee Sandstone has been determined to be mid-Namurian or mid-Arnsbergian to mid-Alportian in age, spanning the bottom ~80% of biozone A (Jones & Truswell 1992).  Three younger glacial intervals were identified by Jones & Fielding (2004).  By assuming a linear sedimentation rate, Jones (2003) calculated that the oldest glacial interval occupies ~1/6 of biozone B, the next glacial interval occupies ~25% of biozone C, and the youngest interval spans the uppermost portion of biozone C and lowermost portion of biozone D.  The mid-Tastubian through mid-Aktastinian (mid-Sakmarian through early Artinskian) age of the Reids Dome Beds is constrained palynologically (see “Northern Galilee Basin”) (Jones & Truswell 1992).

Colinlea Sandstone, Peawaddy Formation, Black Alley Shale & Bandanna Formation  
The age of the Colinlea Sandstone, Peawaddy Formation, Black Alley Shale, and Bandanna Formation is taken from marine biostratigraphic data (Briggs 1998).  The Roadian through Wordian Colinlea Sandstone spans the Echinalosia robusta/hanloni through the E. deari brachiopod biozone (Briggs 1998).  The Capitanian Peawaddy Formation contains brachiopods from the Echinalosia ovalis assemblage (Briggs 1998).  The basal half of the Peawaddy Formation contains outsized clasts.  Therefore, by approximation of a linear sedimentation rate, deposition in the basal half of the formation, during the early to mid-Roadian, is interpreted to have been influenced by distal glaciers.  The latest Capitanian to early Wuchiapingian Black Alley Shale is thought to span the E. voiseyi brachiopod biozone (Briggs 1998).  The early Wuchiapingian through Changhsingian (end Permian) Bandanna Formation does not contains marine fossils but is constrained palynologically to the upper stage 5 or upper APP5 zone (Jones & Truswell 1992; Briggs 1998).   

Bowen Basin

Western Bowen Basin/ Denison Trough

Reids Dome Beds & Cattle Creek Formation
	The top of the mid-Sakmarian through early Artinskian (mid-Tastubian through mid-Aktastinian) Reids Dome Beds is diachronous, ranging from the late Tastubian to mid-Aktastinian (Jones & Truswell 1992).  The formation is constrained palynologically (see “Northern Galilee Basin”).  The youngest base of the Cattle Creek Formation is placed at the base of the Echinalosia curtosa brachiopod zone, according to Briggs (1998), and is constrained by the identification of marine invertebrate fauna within the formation.  Briggs (1998) places the top of the Cattle Creek Formation in the middle of the E. preovalis zone.  Therefore, the Cattle Creek Formation spans the mid-Aktastinian to mid-Baigendzhinian of the Artinskian.  The Cattle Creek Formation contains outsized clasts throughout the thickness of most of the formation, particularly in the lower portion.  Assuming a linear sedimentation rate, glacial influence spans the lower two-thirds of the time period occupied by the Cattle Creek Formation, until the early Baigendzhinian.

Aldebaran Sandstone, Freitag Formation, Ingelara Formation, Catherine Sandstone, Peawaddy Formation, Black Alley Shale, & Bandanna Formation  
The Lower Aldebaran Sandstone, Upper Aldebaran Sandstone, Freitag Formation, Ingelara Formation, Catherine Sandstone, Peawaddy Formation, Black Alley Shale, and Bandanna Formation were plotted in time based on marine biostratigraphic data from Briggs (Briggs 1998).  Briggs (1998) places the Lower Aldebaran Sandstone spanning the mid- Echinalosia preovalis (upper) zone through the top of the E. discinia zone, based on marine invertebrate fauna found throughout the formation (Briggs 1998).  The upper Aldebaran Sandstone (+ “Warranilla Formation”) spans the E. robusta/ hanloni through the top of the P. clarkei  brachiopod biozones (Briggs 1998).  The authors have chosen not to recognize the “Warranilla Formation” and include it with the upper Aldebaran Sandstone.  Brachiopod fauna within the Freitag Formation place it within the P. ingelarensis biozone (Briggs 1998).  The Ingelara Formation contains fauna from the P. crassa brachiopod biozone (Briggs 1998).  The Catherine Sandstone is thought to span the Echinalosia deari zone (Briggs 1998).  Age constraints on the Peawaddy Formation, Black Alley Shale, and Bandanna Formation are discussed above under “Eastern Margin of Galilee Basin.”  Age constraints on the glacial interval within the Peawaddy Formation follow the same logic outlined for the eastern margin of the Galilee Basin.  The Freitag and Ingelara Formations and Catherine Sandstone and equivalents contain evidence of glacially-influenced deposition.

Eastern Bowen Basin/ Northern New England Fold Belt

Campwyn Volcanics/ Rockhampton Group & Neerkol Formation
The late Devonian to early Carboniferous age of the Campwyn Volcanics & the Rockhampton Group is taken from Leitch et al. (1994), which is based on identification of brachiopods from within the formation that place the formation spanning the Schellwienella burlingtonensis to Levipustula levis brachiopod biozones.  The Rockhampton Group contains marine invertebrate fauna that indicate a Tournaisian age (Dear et al. 1971) and is thought to be stratigraphically equivalent to the Campwyn Volcanics (Bryan et al. 2004).  Additionally, U-Pb zircon dates on the upper silicic volcanic deposits of the Campwyn Volcanics yield ages ranging between 360 and 350 Ma (Bryan et al. 2004).  The age of the two oolitic intervals is constrained by biostratigraphic data published in Dear et al. (1971).  The age of the Neerkol Formation is also taken from Leitch et al. (1994).  The formation lacks age diagnostic fauna.  The base of the formation is constrained by biostratigraphic data from the underlying Campwyn Volcanics, but the top of the formation remains unconstrained. 

Youlambie Conglomerate & Carmila Beds 
The age of the Youlambie Conglomerate is taken from Briggs (1998), based on biostratigraphic data from marine intercalations within the formation documented by Dear et al. (1971).  The earliest Asselian to early Artinskian (brachiopod biozones Lyonia bourkei to top of Tomioposis strzeleckii) age was also adopted by Jones & Fielding (Jones & Fielding 2004).  The Youlambie Conglomerate is laterally equivalent to the Carmila Beds (Fielding et al. 1997).  The age of the glacial interval within the Youlambie Conglomerate was established via correlation with the well-dated Boonderoo Beds.  Both the Youlambie Conglomerate and the Boonderoo Beds contain a single discrete interval of glacial facies within a unit of Sakamarian age.  Hence, the glacial interval from both the Boonderoo Beds and the Youlambie Conglomerate were assumed to correlate (Jones 2003; Jones & Fielding 2004).  The age of the Carmila Beds has been most recently revised based on U-Pb SHRIMP date of 294 Ma by Fielding et al. (1997).  This date was obtained using the SL13 standard and was corrected to the current TEMORA standard by adding 1% to the original age, based on recommendations made in Black et al. (2003).  The correction resulted in a new age of 297 Ma.  

Yarrol Formation, Owl Gully Volcanics, Moah Creek Beds & Dinner Creek Conglomerate
The age of the overlying Yarrol Formation and Owl Gully Volcanics is based largely on biostratigraphic data from Dear et al. (1971), revised by Briggs (1998).  The stratigraphic placement of the Moah Creek Beds and Dinner Creek Conglomerate is based partially on lithostratigraphic correlation with the Denison Trough succession (Fielding et al. 1997), and is taken from the stratigraphic scheme published by Briggs (1998).  The age of the top of the Dinner Creek Conglomerate remains biostratigraphically unconstrained.  Exotic outsized clasts in marine mudrock within the Moah Creek Beds were documented during field examination of the unit.  The basal sandstone unit of the Moah Creek Beds contains facies similar to those of the Upper Aldebaran Sandstone.  The interval of glacially-influenced strata sits atop the basal sandstone unit of the Moah Creek Beds, and therefore, thought to be lithostratigraphically and chronstratigraphically equivalent to the Freitag Formation, whose age is biostratigraphically well-constrained in the eastern Galilee Basin and Denison Trough of the Bowen Basin.

Gunnedah Basin

Maules Creek

Boggabri Volcanics, Werrie Basalt, Leard, Goonbri, Maules Creek, Porcupine, Watermark Formations & Black Jack Group `
The age of the Boggabri Volcanics, Werrie Basalt, Leard Formation, Goonbri Formation, Maules Creek Formation, Porcupine Formation, Watermark Formation, and Black Jack Group is taken from Briggs (1998), which is based on available palynological  and marine invertebrate data for each of the formations (Tadros 1993).  Examination of the Goonbri, Porcupine, and Watermark Formations in core and/or in outcrop reveals the presence of glacial facies at intervals in these formations.  Additionally examination of photographs and description of core detailed in Hamilton (1993), reveal diamictites or “clast-rich muddy sandstones” that appear to contain basement clasts in the shallow marine, Arkarula member of the Black Jack Formation, which is misinterpreted as “tidal channel facies” in Hamilton (1993).  Biostratigraphic diagnosis places the formation spanning the P. crassa and the lower portion of the E. deari brachiopod biozones (Briggs 1998).  Furthermore, Tadros (1993) lithostratigraphically correlates the Arkarula member to the Kulnura Marine Tongue in the Newcastle Coalfield and the lower half of the Arkarula member to the Marangaroo Conglomerate in the Western Coalfield and Erins Vale Formation in the Southern Coalfield.

Southern New England Fold Belt

Rocky Creek Syncline

Luton & Namoi Formations
The age of the Luton Formation is constrained by biostratigraphic data from numerous sources.  McKelvey and McPhie (1985) refer to brachiopods of the Tulcumbella tenuistriata zone near the base of the type section of the Luton Formation and faunas of the Schellwienella burlingtonensis zone in the upper portion of the unit.  Conodont data confirm an early to late Tournaisian age (Mory 1981).  Study of brachiopod fauna from the formation by Roberts et al. (1993a) also constrains the top of the formation within the Schellwienella burlingtonensis zone, during the late Tournaisian.  The Namoi Formation contains brachiopods of the Inflatia elegans subzone (McKelvey & McPhie 1985).  Biostratigraphic studies of the formation, including Roberts et al. (1993a) and Roberts (unpubl. data), indicate that the Namoi Formation spans the mid-Schellwienella burlingtonensis through early Orthotetes australis brachiopod zones, the G. texanus to S. anchoralis conodont zones, or late Tournaisian to earliest Visean.  

Caroda Formation
The age of the Caroda Formation is constrained biostratigraphically and radiometrically.  Opdyke et al. (2000) reference mid-Visean marine fossils within the formation.  The Caroda Formation contains conodonts from Montognathus semicarinatus and Montognathus carinatus zones and brachiopods from the Delepinea aspinosa brachiopod zone (Jenkins et al. 1993; Roberts et al. 1993a).  Roberts et al. (1993a) and Roberts (unpubl. data) place the base of the formation in the middle of the Orthotetes australis brachiopod zone.  Additionally, a radiometric U-Pb SHRIMP date on the Barney Springs Andesite within the formation yields an age of 342 +/- 3.5 Ma (AS3: corrected TEMORA age 338.6 Ma).    The age of the top of the formation is poorly constrained.  While traditional stratigraphic models infer a disconformable contact between the Caroda Formation and the overlying Spion Kop Conglomerate, field examination of the contact suggests that it may be conformable and even gradational.

Spion Kop Conglomerate
The early Namurian (mid-Pendleian) age of the top of the Spion Kop Conglomerate is constrained radiometrically by U-Pb SHRIMP dating of ignimbrites in the overlying Clifden Formation (see following discussion).  The Spion Kop Conglomerate contains glacial evidence in the form of diamictite units at its base and top and is illustrated by two thin glacial intervals within the Spion Kop Conglomerate.  The base of the unit is poorly constrained.  The entire Spion Kop Conglomerate is thought to be restricted to the Serpukhovian/Namurian because late Visean (Marginirugus barringtonensis brachiopod zone) oolitic limestones are found in Queensland (Roberts, pers. comm.), which is generally inconsistent with cold, glacial conditions.  Additionally, there is no evidence of Visean glaciation from other localities in eastern Australia.  However, the Spion Kop Conglomerate could extend into the Visean. 

Clifden Formation  
The age of the Clifden Formation is well-constrained radiometrically.  Eight U-Pb SHRIMP dates using either the SL13 or AS3 standard were obtained on seven ignimbrite units found within the formation (Opdyke et al. 2000; Roberts et al. 2003).  Each corrected age is plotted in time on the stratigraphic framework, immediately to the right of the Clifden Formation.  The resulting ages range from 325.5 Ma to 317.9 Ma and constrain the formation to early Serpukhovian to mid-Bashkirian (Namurian) according to the Gradstein et al. (2004) timescale.  The terrestrial Clifden Formation also contains Nothorhacopteris and Sphenopteridium intermedium floras (Roberts et al. 2003). 

Rocky Creek Conglomerate 
	Published radiometric dates on the Plagyan Ignimbrite member and the Pound Rock Rhyodacite member of the Rocky Creek Conglomerate were corrected from the AS3 standard to the TEMORA standard (-1%) to yield ages of 315.8 and 316.8 Ma, respectively.  The age of the top of the Rocky Creek Conglomerate is constrained by radiometric dates obtained from the Eulowrie Pyroclastic member of the Lark Hill Formation (310.6 +/- 4 Ma SL13  313.7 Ma TEMORA), which immediately overlies the Rocky Creek Conglomerate (Opdyke et al. 2000; Roberts et al. 2003).  Additionally, U-Pb SHRIMP dating of the Tops Rhyolite Member yield an age of 316.3 +/- 2.1 Ma (AS3: 313.8 Ma using TEMORA standard) (Roberts et al. 2003).  Roberts et al. (2003) report Nothorhacopteris flora from the mid-Bashkirian through Moscovian (Westphalian) Lark Hill Formation.  The age of the top of the formation is poorly constrained.

Werrie Syncline

Tulcumba Sandstone, Namoi & Merlewood Formations
The early Tournaisian age of the Tulcumba Sandstone is constrained by biostratigraphic data.  The formation contains brachiopods of the Tulcumbella tenustriata and Spirifer sol zone and conodonts of the Lower crenulata through Upper crenulata zones (Roberts 1975; McKelvey & McPhie 1985; Roberts et al. 1993a).  The overlying Namoi Formation in the Werrie Syncline sections contain brachiopods that belong to the Spirifer Sol and Schellwienella burlingtonensis zones, placing it entirely in the Tournaisian, which is slightly older than the age of the formation in the Rocky Creek Syncline sections.  The Merlewood Formation contains brachiopods that are early to late Visean in age from the Gigantoporductus tenuirugosus and Inflatia elegans subzones and the Orthotetes australis zone (McKelvey & McPhie 1985; Roberts unpubl. data).  Roberts et al. (2006) report U-Pb SHRIMP dates on three ignimbrite members within the Merlewood Formation: Isismede Ignimbrite Member, Burnewang Ignimbrite Member, and Wheelihans Gap Ignimbrite Member.  Multiple dates on each member were averaged and then corrected by -1% from AS3 standard to TEMORA standard, yielding ages of 348.5, 339.6, and 323.7 Ma, respectively.  The date on the Isismede Ignimbrite is slightly old and conflicts with biostratigraphic data from the Namoi Formation.  However, a diachronous boundary between the Namoi and Merlewood Formation is likely, as the Merlewood is either gradiational, conformable, or disconformable at different locations (McKelvey & McPhie 1985).  The base of the Merlewood Formation may, in fact, be slightly older in the region where the Isismeda Ignimbrite is exposed.  However, the authors have chosen to base formation ages primarily on available biostratigraphic data from the Namoi Formation rather than the radiometric dates from the Merlewood Formation.

Currabubula Formation
	The Currabubula Formation is known to contain Rhacopteris flora and the microflora from the Potonieisporites assemblage (Whetten 1965; Helby 1969).  Its latest Serpukhovian to mid-Moscovian age (mid-Namurian to mid-Westphalian) is constrained radiometrically.  U-Pb SHRIMP dates on five laterally extensive and mappable ignimbrite members throughout the formation yield dates (corrected to TEMORA standard) ranging from 308.9 to 316.7 Ma (Flood et al. 1993; Opdyke et al. 2000; Roberts et al. 2004; Roberts et al. 2006; Roberts unpubl. data).  The exact age of the top and base of the formation are uncertain.  However, in some cases, discrete stratigraphic intervals within the formation containing glacial facies can be placed stratigraphically relative to mappable and dated ignimbrites in order to tightly constrain the age of discrete glacial events.  The stratigraphically lowest ignimbrite, the Figtree Creek Ignimbrite has been dated to 313.6 +/- 3.6 Ma (S13: corrected to TEMORA age 316.7 Ma) (Opdyke et al. 2000; Roberts unpubl. data).  The Taggarts Mountain Ignimbrite, which is stratigraphically higher than the Figtree Creek Ignimbrite yielded a U-Pb SHRIMP date of 319.3 +/- 2.8 Ma (AS3: corrected to TEMORA age 316.1 Ma) (Roberts et al. 2004; Roberts unpubl. data).  A documented glacial interval at Cana Creek lies directly below the Taggarts Mountain Ignimbrite, but stratigraphically above the Cana Creek Tuff and the Figtree Creek Ignimbrite Member.  Therefore, it is constrained to a mid-Bashkirian or earliest Westphalian age.  The documented glacial interval within the Rosedale member at Currabubula Creek lies stratigraphically below the Cana Creek Tuff, which lies stratigraphically between the Figtree Creek Ignimbrite and the Taggarts Mountain Ignimbrite.  Hence, the Rosedale member is the oldest glacial interval and is plotted in the mid-Bashkirian or latest Namurian because it must be older than the Taggarts Mountain Ignimbrite and the glacial interval at Cana Creek.  The age of the base of the Rosedale member is unknown.  Finally, a radiometric date on the youngest ignimbrite near the top of the formation, the Piallaway Trig Ignimbrite Member, yields an age of 306.0 +/- 4.2 Ma (SL13: corrected to TEMORA age 309.1 Ma) (Opdyke et al. 2000; Roberts et al. 2004; Roberts unpubl. data).  The final glacial interval identified within the Currabubula Formation lies stratigraphically above the Piallaway Trig Ignimbrite Member and near the top of the formation, placing it in the mid-Moscovian (late Westphalian).  The age of the top of the formation and, hence, the age of the end of the final of the three glacial intervals remains poorly constrained.

Woodton, Temi Formations & Werrie Basalt
	The age of the Woodton and Temi Formations and the Werrie Basalt are taken from Roberts et al. (2006).  The Woodton Formation contains Gangomopteris and Noegerrathiopsis flora (Whetten 1965; Roberts et al. 2006).  The Brogans Rhyodacite, from within the Woodton Formation is dated at 290.5 +/- 2.8 Ma (AS3: 287.6 Ma TEMORA), or a mid-Sakmarian age for the Woodton Formation.

Rouchel Block

Kingsfield, Goonoo Goonoo, Dangarfield, waverly formations & Brushy Hill Limestone
	The age of the Kingsfield, Goonoo Goonoo, Dangarfield, and Waverly Formations and the Brushy Hill Limestone is based on brachiopod and conodont biostratigraphic data published in Roberts et al. (1993a; 1995a) and Roberts (1985).  Additionally, formation boundaries were drafted based on Roberts (unpubl. data).  U-Pb radiometric dating of an ignimbrite member within the Kingsfield Formation (355.8 +/- 5.6 Ma SL13 359.3 Ma TEMORA) and of the Foybrook Andesite Member of the Waverly Formation (350.9 +/- 4.0 Ma SL13 354.4 Ma TEMORA) were plotted to aid in constraining the age of the succession (Roberts et al. 1995a; Roberts unpubl. data).  These converted ages are in agreement with the previously established biostratigraphic data.

Isismurra Formation & Gilmore Volcanics
	The terrestrial volcaniclastic early to mid-Visean Isismurra Formation is dated radiometrically and can be stratigraphically correlated with laterally equivalent or interfingering marine units in which better biostratigraphic control is available, such as the Woolooma Formation (Roberts 1985; Roberts et al. 1995b).  The Curra Keith Tongue lies at the base of the formation.  U-Pb SHRIMP dates on the member yield an AS3 age of 349.6 +/- 1.7 Ma (346.1 Ma TEMORA) and an SL13 date of 342.1 +/- 3.2 Ma (345.5 Ma TEMORA) (Roberts et al. 1995a; Roberts et al. 2006).  Two dates on unnamed red ignimbrites within the formation were averaged and converted to 343.1 Ma (TEMORA) (Roberts et al. 2006; Roberts unpubl. data).  The Martins Creek Andesite is a geographically widespread unit that sits as the stratigraphically lowest ignimbrite in the Gilmore Volcanic Group and the second highest ignimbrite in the Isismurra Formation.  It has been dated at 332.3 +/- 2.2 Ma (SL13) and converted to 335.6 Ma (TEMORA) (Roberts et al. 1995a; Roberts unpubl. data).  

Mt. Johnstone Formation & Paterson Volcanics
The age of the Mt. Johnstone Formation is constrained biostratigraphically, with further constraint via radiometric dates on the overlying Paterson Volcanics.  The Mt. Johnstone Formation contains the first occurrence of the Nothorhacopteris macroflora and the Grandispora maculosa palynoflora assemblage (Kemp et al. 1977; Playford 1985; Claoue-Long et al. 1995).  Jones & Truswell (1992) place the G. maculosa assemblage in the late Visean to earliest Namurian (mid-Asbian through Pendelian).  Therefore, the unconformable base of the Mt. Johnstone Formation (Roberts et al. 1995a) is placed in the mid-Asbian, which is consistent with radiometric age constraints on the underlying Gilmore Volcanics and Isismurra Formation.  The top of the Mt. Johnstone Formation is placed in the mid-Brigantian, due to a radiometric age of 328.5 +/- 1.4 Ma on the overlying Paterson Volcanics (Claoue-Long et al. 1995; Roberts et al. 1995b).  Four independent zircon age measurements on the Paterson Volcanics using both ID-TIMS and SHRIMP techniques produced statistically indistinguishable dates that converge upon the cited age of the Paterson Volcanics (Claoue-Long et al. 1995). 

Seaham Formation 
The Seaham Formation on the Rouchel Block is thought to unconformably overlie the Paterson Volcanics (Roberts et al. 1995b).  Biostratigraphic control on the age of the formation is sparse and only includes the identification of the Potonieisporites palynoflora assemblage by Helby (1969), which corresponds to the Jones & Truswell’s (1992) palynological Biozone D.  Jones (Roberts et al. 1995a; Roberts et al. 1995b) restricts the Potonieisporites assemblage to the mid- to late Westphalian.  Numerous radiometric dates have been obtained on laterally extensive and widespread ignimbrites throughout the formation (Roberts et al. 1995a; Roberts et al. 1995b; Roberts et al. 2006).  Listed in order from oldest to youngest, SHRIMP and/or IDTIMS U-Pb dates were obtained on the following five ignimbrites located on the Rouchel Block within the Seaham Formation: 1) Mirannie Ignimbrite Member (321.3 +/- 4.4 Ma SL13 converted to 324.4 Ma TEMORA), 2) Elmswood Ignimbrite Member (326.4 +/- 2.9 Ma AS3 converted to 323.1 Ma TEMORA), 3) Kewell Creek Ignimbrite Member (320.5 +/- 2.9 AS3 converted to 317.3 TEMORA), 4) Matthews Gap Dacite Member (309.0 +/- 3.0 IDTIMS), and 5) Well Gully Ignimbrite Member (305.7 +/- 2.7 AS3 converted to 302.6 TEMORA).  This places the Seaham Formation from earliest Serpukhovian to late Kasimovian (earliest Namurian to latest Stephanian).  
Sussmilch & David (1919) described a complete section of the Seaham Formation at Seaham, and defined it as the type section.  Their description documents glacially-influenced deposition in the formation, including “tillite” and “varved shale” facies with small outsized clasts.  Our field investigations could not reproduce this section, due to deterioration in the quality and extent of exposure.  Thus, we have been forced to rely largely on the well-documented accounts of the formation by Sussmilch & David (1919).  Sussmilch & David’s (1919) lithologic description of the “tillite” facies matches the modern-day usage of the “diamictite” lithology.  Additionally, Sussmilch & David (1919) note “varved shales”, part of which are poorly exposed today in what is left of the Seaham quarry.  Sussmilch & David (1919) describe three intervals of strata that contain “tillite” or “varved shales” (determined to be “glacially-influenced facies).  Without proper age constraint, the authors hypothesize that these three glacial intervals correspond to the three younger Carboniferous glacial intervals C2, C3, and C4.  The age of the C2-C4 glacial intervals are well-constrained using the stratigraphic position glacially-influenced strata from various formations relative to radiometrically dated ignimbrites.  It is unlikely that the oldest glacial interval, C1, is recorded in the Seaham Formation as the base of the Seaham Formation contains a thick succession of conglomerate, free of direct evidence of glacially-influenced facies (Sussmilch & David 1919).  

Cranky Corner/ Gresford Block

Wallaringa Formation, Gilmore Volcanics, Mt. Johnstone Formation & Paterson Volcanics
	The Carboniferous stratigraphy of the Gresford Block is similar to that of the Rouchel Block, with a few exceptions.  The Wallaringa Formation is the lateral equivalent of the Isismurra Formation, containing brachiopods from the Inflatia elegans and Linoprotonia tenuirugosa subzones of the Delepinea aspinosa zone (Roberts et al. 1995a; Roberts unpubl. data).  Additionally, the formation contains spores and pollen from the Grandiospora maculosa zone (Kemp et al. 1977).  The age of the top of the formation is constrained radiometrically by the date on the overlying Martins Creek Ignimbrite, at the base of the Gilmore Volcanic Group (see discussion in previous “Rouchel Block” section) (Roberts et al. 1995a; Roberts unpubl. data).

Seaham & Tamby Creek Formations
	The top of the Seaham Formation in the Cranky Corner region and Gresford Block is thought to be younger than in the Rouchel Block, based on radiometric ages from within the Seaham Formation and the overlying Tamby Creek Formation.  Four dated ignimbrites from oldest to youngest within the Seaham Formation that occur in the Cranky Corner region and Gresford Block include: 1) Mirannie Ignimbrite Member (321.3 +/- 4.4 Ma SL13 converted to 324.4 Ma TEMORA), 2) Webbers Creek tuff (313.9 +/- 3.0 Ma SL13 converted to 317.0 Ma TEMORA), 3) Lochinvar tuff (310.6 +/- 4.0 Ma SL13 converted to 313.7 Ma TEMORA, and 4) Mount Durham tuff (306.5 +/- 2.1 Ma SL13 converted to 309.5 Ma TEMORA (Roberts et al. 1995b; Claoue-Long & Korsch 2003; Roberts unpubl. data).  This places the Seaham Formation in the Serpukhovian through mid-Moscovian (Namurian through late Westphalian).  Age constraint on the observed interval of glacial strata within the Seaham Formation at Six Mile Quarry is poor.  Based on the mapped extent of the formation and the location of the exposure of the glacial interval, the glacial interval appears to be in the middle of the formation and is located on the western edge of the Myall Block.  There are no dated ignimbrites present that might aid in constraining the age of the interval.  However, the exposures of glacial strata from the Johnson’s Creek Conglomerate are < 40 km away from the glacial interval within the Seaham at Six Mile Quarry.  Therefore, it is likely that the glacial interval exposed within the Seaham at Six Mile Quarry is coeval with the Johnson’s Creek Conglomerate, placing the glacial interval in the late Serpukhovian (mid-Namurian).  The mid-Moscovian to mid-Kasimovian (late Westphalian to late Stephanian) age of the overlying terrestrial volcanoclastic Tamby Creek Formation has been established via radiometric age constraints alone, as no biostratigraphic data are available from this Formation (Archbold 2003; Balme & Foster 2003).  The oldest and youngest ignimbrite within the formation yield converted TEMORA ages of 306.7 and 303.3 Ma (original 300.3 +/- 2.4 and 303.7 +/- 2.4 Ma using SL13 standard) (Claoue-Long & Korsch 2003; Roberts unpubl. data). 

Dalwood Group: Beckers Formation, Cranky Corner Sandstone & Billy Brook Formation
	The Permian Dalwood Group, Greta Coal Measures and Maitland Group stratigraphy is recognized in the Cranky Corner region, which is a structural outlier of the nearby Sydney Basin.  The age of the Beckers Formation, Cranky Corner Sandstone, and Billy Brook Formation is based on marine invertebrate and palynological data from the formations (Archbold 2003; Balme & Foster 2003).  A compromise was plotted where the data conflict.  The Beckers Formation spans the entire APP 1.22 and most of the APP2.1 palynological zones (Balme & Foster 2003).  The basal half of the formation was determined to contain evidence of glacial facies, based on core examination and description.  Therefore, a linear sedimentation rate for the formation was assumed and a late Asselian to early Sakmarian (Shikhan to mid-Tastubian) glacial interval was plotted.  The Cranky Corner Sandstone spans the upper portion of the APP2.1 and basal portion of the APP2.2 palynological zone.  The Billy Brook Formation is thought to be Aktastinian (early Artinskian) according to data from pollen and spores within the formation (Balme & Foster 2003).  Corrected radiometric dates on two unnamed tuffs from the Beckers Formation and Cranky Corner Sandstone plot within the biostratigraphic age constraints, with dates of 287.1 +/- 2.4 Ma (SL13) converted to 290.0 Ma (TEMORA) and 284.1 +/- 2.2 Ma (SL13) converted to 287.0 Ma (TEMORA) from each formation, respectively (Claoue-Long & Korsch 2003).  The authors’ have documented an 11 m thick discrete interval of strata at the base of the Billy Brook Formation in DM Tangorin-DDH1 borehole that displays evidence of glacial conditions.  Assuming a linear sedimentation rate, the thickness of this interval relative to the thickness of the entire formation was converted to time and placed as a glacial interval at the base of the formation.

Greta Coal Measures & Maitland Group
	The authors have chosen to place the Greta Coal Measures in the Baigendzhinian through Filippovian (late Artinskian through early Kungurian) based on biostratigraphic and radiometric age constraints on the formation boundaries.  Briggs (1998) places the Greta Coal Measures in the upper and lower Echinalosia preovalis brachiopod zones, based on brachiopod biostratigraphic data from the underlying and overlying units.  Additionally, Balme & Foster (2003) note moderately preserved pollen and spores within the Greta Coal Measures from palynological zone APP3.1.  Because the upper portion of the APP3.1 zone spans the lower Baigendzhinian, the authors’ placement is consistent with the palynological data.  We have chosen to extend the top of the formation beyond the top of the E. preovalis brachiopod zone into most of the E. maxwelli zone due radiometric age data from Roberts et al. (1996).  Roberts et al. (1996) publish two U-Pb SHRIMP dates, one from below the top of the Greta Coal Measures (268.9 +/- 2.0 Ma, SL13 271.6 Ma TEMORA) and one just above the base of the Branxton Formation (272.2 +/- 3.2 Ma, SL13  274.9 Ma TEMORA) (Roberts et al. 1996).  Unfortunately, the corrected dates disobey the stratigraphic order of the succession.  In order to account for some of the error, the authors averaged the two original SL13 dates and applied a +1% correction to the average in order to convert from SL13 to TEMORA standard and provide a rough estimation of the age of the top boundary of the Greta Coal measures.  Admittedly, this solution does not provide optimal precision and accuracy.  However, the resulting date of 272.7 Ma for the Greta Coal Measures/ Branxton Formation boundary places the overlying Branxton Formation within the range of biostratgraphic data for the formation, which contains E. maxwelli fauna (Briggs 1998).  Placing the top boundary of the Greta Coal Measures within the upper portion of the E. maxwelli zone satisfies both the radiometric and biostratigraphic age constraints available.
	The age of the overlying Maitland Group, which includes the Branxton Formation, was determined from biostratigraphic data published in Briggs (1998), which places the top of the formation at the top of the E. wassi brachiopod biozone, at the top of Roadian.  The biostratigraphic and radiometric age constraints on the base of the formation are discussed in the previous paragraph.  Units within the Maitland Group all show evidence of glacial facies, with the exception of the basal fluvial Jasdec Park Sandstone Member of the Branxton Formation.  The duration of the Jasdec Park Sandstone Member is estimated from its approximate thickness.   

Western Myall Block

Wooton Beds, Conger Formation & Nerong Volcanics 
	The stratigraphic placement of units in time in the Myall Block is based primarily on biostratigraphic data and secondly on radiometric dates on volcanic members.  The Wootton Beds contain brachiopod fauna from the S. burlingtonensis, O. australis, and Inflatia elegans assemblages, placing the formation in the late Tournaisian to mid-Visean (Roberts et al. 1995a; Roberts unpubl. data).  Conger Formation overlies the Wootton Beds in some areas but is coeval in others.  Brachiopod fauna within the Conger Formation place it within the L. tenuirugosa subzone (Roberts et al. 1995a; Roberts unpubl. data).  A U-Pb SHRIMP date using both the SL13 standard on the overlying Nerong volcanics yield dates of 338.4 +/- 4.6 Ma.  This date was left uncorrected because applying the correction results in an age that is older than the biostratigraphic data suggest, as discussed in the first section of this appendix.

Berrico Creek, Faulkland, Karuah, Booral, & McInnes Formations   
The age of the mid-Visean Berrico Creek, late Visean Faulkland, late Visean Karuah, early Serpukhovian (early Namurian or Pendleian) Booral and mid-Serpukhovian (early to mid-Namurian or early Arnsbergian) McInnes Formations are taken from Roberts et al. (1995a) and are based on brachiopod biostratigraphic data.  The Berrico Creek Formation occupies the Rhipidomella fortimuscula and the basal portion of the Marginirugus barringtonensis biozones (Roberts 1985; Roberts et al. 1995a; Roberts et al. 1995b; Roberts unpubl. data).  The Faulkland and Karuah Formations occupy the majority of the Marginirugus barringtonensis biozone (Roberts et al. 1995a; Roberts unpubl. data).  Both the McInnes and Booral Formations contain brachiopods belonging to the Levipustula levis biozone.  Additionally, the McInnes Formation contains a palynoflora that is equated to the S. ybertii- D. birkheadensis palynozone, further asserting its mid-Serpukhovian (early to mid-Namurian or early Arnsbergian) age (Roberts 1975; Roberts et al. 1995b).  

Johnsons Creek Conglomerate
The mid- to late Serpukhovian (mid-Namurian or mid-Arnsbergian) Johnsons Creek Conglomerate contains Sphenopteridium sp. plant specimens, which suggests the presence of an enriched Nothorhacopteris flora.  Additionally, the correlative Muirs Creek Conglomerate contains poorly preserved S. ybertii- D. birkheadensis palynoflora of similar age as the McInnes Formation underlying the Johnsons Creek Conglomerate.  U-Pb SHRIMP dates on two tuffs within the Johnsons Creek Conglomerate reveal ages of 323.2 +/- 3.2 and 321.9 +/- 4.0 Ma (SL13) (Roberts et al. 1995b).  The older of the two ages provides an upper age constraint on the age of the Levipustula levis brachiopod biozone.  However, the date contradicts reasonable stratigraphic constraints on the biozone throughout the region.  A further understanding of the age of the top of the Levipustula levis biozone is necessary.  The Johnsons Creek Conglomerate contains evidence of glacially-influenced deposition in the form of diamictite.

Alum Mountain Volcanics, Dewrang Group & Gloucester Coal Measures
	The Alum Mountain Volcanics disconformably overlie the Johnsons Creek Conglomerate, with a prominent unconformity in the middle of the unit.  The upper Lakes Road Rhyolite member has been dated radiometrically at 274.1 +/- 3.4 Ma (SL13: 276.8 Ma TEMORA) (Roberts et al. 1995b; Roberts unpubl. data).  The age of the lower members is poorly constrained, relying only on the presence of Glossopteris and Gangamopteris macroflora, widely ranging palynological data that indicate a broad early Permian (palynozones 3 and 4) age range, and loose lithostratigraphic correlations (Roberts et al. 1995b; Briggs 1998).   The age of the early Kungurian through late Roadian Dewrang Group and the late Roadian through mid-Wordian Gloucester Coal Measures is based on palynostratigraphic data (Roberts et al. 1996).  The Dewrang Group contain pollen that place it in the APP3.3, APP4.1 and APP4.2 zones (Roberts et al. 1996).  The Greta Coal Measures contain spores from the APP4.3 zone (Roberts et al. 1996).  

Eastern Myall Block

Wang Wauk Formation, Darts Creek Mudstone, Wallanbah Formation, Kataway Mudstone, Boolambayte Formation
The Darts Creek Mudstone and underlying Wang Wauk Formation do not contain age diagnostic flora or fauna.  However, the age of the top boundary of the Darts Creek Mudstone is loosely constrained by biostratigraphic data from the overlying formation.  The Wallanbah Formation contains brachiopods of the S. burlingtonensis zone and conodonts belonging to the Siphonodella crenulata and Scaliognathus anchoralis zones, restricting the formation to the middle to late Tournaisian (Roberts 1985; Roberts et al. 1995b).  The Kataway Mudstone also contains S. anchoralis zone conodonts and is given a latest Tournaisian to earliest Visean age (Roberts 1985; Roberts et al. 1995a; Roberts unpubl. data).  The age of the early Visean Boolambayte Formation is constrained based on the presence of brachiopods from the O. australis and R. fortimuscula zones (Roberts 1985; Roberts unpubl. data).  The age of the overlying Nerong Volcanics is constrained radiometrically, as discussed in the “Western Myall Block” sections. 

Booti Booti Sandstone & Yagon Siltstone
	The Booti Booti Sandstone unconformably overlies the Nerong Volcanics and/or the Boolambayte Formation and contains M. barringtonensis zone brachiopods, constraining the formation to the late Visean (mid-Brigantian) (Roberts 1985; Roberts et al. 1995a).  The overlying Yagon Siltstone also contains brachiopods of the M. barringtonensis zone but also the Levipustula levis zone, placing the formation in the latest Visean to early Namurian (late Brigantian through Pendleian) (Roberts 1985; Roberts et al. 1995a).  A U-Pb SHRIMP date on the volcanic Violet Hills Member of the Yagon Siltstone revealed an age of 330.6 +/- 4.6 Ma, using the SL13 standard.  Unfortunately, the radiometric date indicates an older age than that surmised from the known biostratigraphic data from the formation.  The biostratigraphic and radiometric data can not be reconciled.  The authors chose to honor the biostratigraphic age constraints on the formation.  A glacial interval has been plotted in the middle of the Yagon Siltstone because the authors identified indirect evidence of glaciation in the middle portion of the formation, and estimated a linear sedimentation rate throughout the formation.

Koolanock Sandstone, Muirs Creek Conglomerate, Alum Mountain Volcanics, Dewrang Group, & Gloucester Coal Measures  
The age of the Koolanock Sandstone is constrained by biostratigraphic data from the overlying and underlying formations.  The age of the overlying Muirs Creek Conglomerate contains poorly preserved S. ybertii- D. birkheadensis and is lithostratigraphically correlated with the radiometrically dated Johnsons Creek Conglomerate (Roberts et al. 1995b).  The mid- to late Serpukhovian (mid-Namurian or mid-Arnsbergian) age of the Muirs Creek Conglomerate is taken from Roberts et al. (1995b) and Roberts (unpubl. data).  The age constraints on the overlying Permian Alum Mountain Volcanics, Dewrang Group, and Gloucester Coal Measures are as for the western Myall Block (see above). 
  
Southern Hastings Block

Quintoc Group:  Kindee Conglomerate, Nevann Siltstone & Hyndmans Creek Formation 
	The Carboniferous and Permian stratigraphy of the Southern Hastings Block is taken from Roberts et al. (1995c), which is based largely on brachiopod biostratigraphic data.  The Kindee Conglomerate is assigned an early Tournaisian age based on lithostratigraphic correlation with a laterally equivalent unit, the Rollans Road Formation, that contains age-diagnostic radiolarians (Roberts et al. 1995c; Roberts unpubl. data).  The early Tournaisian age of the Nevann Silstone is constrained by biostratigraphic data in the overlying Pappinbarra Formation, a limestone unit that contains conodonts from the S. anchoralis and Gnathodus texanus zone along with brachiopods from the S. burlingtonensis zone (Roberts et al. 1995c).  The age of the overlying Hyndmans Creek Formation is poorly constrained, but is placed in the early Visean by Roberts (unpubl. data). 

Mingaletta Formation & Manning Group   
	The Mingaletta Formation is thought to be Namurian in age (Roberts et al. 1995c; Roberts unpubl. data).  It contains brachiopods from the Levipustula levis assemblage and Nothorhacopteris macroflora (Roberts et al. 1995c).  A U-Pb SHRIMP date on a tuff from within the formation yields and age of 326.3 +/- 3.4 Ma, using the SL13 standard (Roberts et al. 1995c), which is within the biostratigraphic age constraints for the formation.  The Asselian Manning Group contains brachiopods from the Lyonia bourkei brachiopod zone (Roberts et al. 1993b).   

Northern Hastings Block

Boonanghi Beds, Majors Creek, Kullatine & Youdale C Formations
	The stratigraphy of the northern Hastings Block is taken from Lennox & Roberts (1988) and has since been updated by Roberts using unpublished radiometric and biostratigraphic data.  The Boonanghi Beds contain fossil fragments of late Devonian to early Carboniferous age (Lennox & Roberts 1988).  The overlying Majors Creek Formation contains brachiopods from the Levipustula levis assemblage in the upper part of the formation, placing it in the late Visean to early Namurian according to the most recent placement of brachiopod biozones relative to the international time scale (Lennox & Roberts 1988; Roberts unpubl. data).  Levipustula levis is also found in the Kullatine and Youdale C Formations (Lennox & Roberts 1988; Roberts unpubl. data), restricting them to an early Namurian age.  In the northwestern Hastings Block, in the Kunderang Gorge region, the Youdale C Formation overlies the Kullatine Formation.  In other localities to the east, it is thought that the Youdale C is partially equivalent to the Kullatine Formation (Roberts unpubl. data).  Therefore, a diachronous contact between the two formations is depicted.  The Kullatine Formation also contains Cravenoceras kullatinense ammonite fossils at the base of the formation and Nothorhacopteris macroflora (Lennox & Roberts 1988).  The upper 350m of the formation (roughly the upper half of the formation) is reported to contain diamicitite (Lindsay 1966; Roberts unpubl. data).  This report was confirmed upon field examination by the authors.  Therefore, a linear sedimentation rate was assumed and a glacial interval was placed in the mid-Namurian or mid-Arnsbergian within the Kullatine Formation.  An outsized clast horizon was identified near the base of the Youdale C Formation.  Assuming a linear sedimentation rate, a mid-Namurian or late Arnbergian glacial interval was estimated.

Youdale B & Youdale A Formations, Yessabah Limestone & Parrabel Beds/Warbro Formation  
The age of the Permian succession is based on unpublished biostratigraphic data (Roberts unpubl. data).  The Youdale B Formation contains brachiopods from the Asselian Lyonia bourkei assemblage (Briggs 1998; Roberts unpubl. data).  The formation is composed entirely of diamictite that is interpreted to be glacial in origin.  The overlying Youdale A Formation does not yield fossil specimens.  Its Sakmarian age is based on biostratigraphic data from the overlying Yessabah Limestone and underlying Youdale B Formation.  The early Artinskian (Aktastinian) Yessabah Limestone contains brachiopods from Echinalosia warwicki (Roberts unpubl. data).  Based on further biostratigraphic data, Briggs (1998) depicts the Yessabah Limestone spanning the E. curtosa, E. warwicki, E. preovalis (lower) and the bottom portion of the E. preovalis (upper).  The overlying Warbro Formation and laterally equivalent Parrabel Beds are placed in the late Artinskian (Baigendzhinian) and taken from Briggs (1998) and Roberts’ (unpubl. data) schemes.  The Parrabel Beds contain Permian brachiopods, bryozoans, and sponge spicules, but provide little age diagnostic data (Lennox & Roberts 1988).  Therefore, the age of the top of these formations is poorly constrained.  However, Briggs (1998) places them in the upper portion of the E. preovalis (upper) biozone. 
  
Sydney Basin

The stratigraphy of the Sydney Basin is taken largely from Briggs (1998), which was constructed based on compilation of biostratigraphic data, with alterations to some formation boundaries based on lithostratigraphic correlation in units that contain few biostratigraphic indicators.

Northwestern Sydney Basin

Unnamed Diamictite, Undifferentiated Shoalhaven Group, Berry Siltstone
Permian units in the northwestern Sydney Basin are locally referred to as the Western Coalfield.  In areas near Ilford and Kandos, we observed an unnamed diamictite unit lying unconformably on early Paleozoic basement.  The unit occupies the base of the Shoalhaven Group in this region (Dunhulty & Packham 1962; McElroy et al. 1969).  The age of the Shoalhaven Group is tightly constrained by biostratigraphy in the eastern part of the Sydney Basin.  By lithostratigraphic correlation to the eastern Sydney Basin, the Shoalhaven Group spans the late Sakmarian through Roadian (B. walkomi through E. wassi brachiopod biozones) (Tye et al. 1996; Briggs 1998).  The late Sakmarian to early Artinskian age of the unnamed diamictite unit is only an estimate based on its stratigraphic location at the base of the Shoalhaven Group and evidence for extensive glaciation during this time interval in many other localities across eastern Australia.  The age of the Berry Siltstone is based on lithostratigraphic correlation to the eastern Sydney Basin, where the marine unit is well-dated biostratigraphically (Briggs 1998).  The Berry Siltstone is composed entirely of diamictite and siltstone with abundant outsized clasts, and is therefore thought to record glacially-influenced deposition.

Illawarra Coal Measures: Nile, Cullen-Bullen, Charbon, and Wallerawang Sub-Groups
	The stratigraphy of the Roadian through Changhsingian (early Guadalupian through Lopingian) Illawarra Coal Measures in the western Coalfield, such as the Nile, Cullen Bullen, Charbon, and Wallerawang Sub-Groups, is taken from coal seam and lithostratigraphic correlations to the eastern Sydney Basin published by Hutton et al. (1990).  The stratigraphy in the eastern part of the basin is constrained biostratigraphically, as compiled by Briggs (1998).  The authors documented two short intervals of siltstone containing outsized clasts in the Glen Davis/Newnes Formation and Baal Bone Formation, both belonging to the Charbon Sub-Group.  These formations are thought to be stratigraphically equivalent to the uppermost Wilton Formation (Tongarra Coal) and the Bargo Claystone (Hutton et al. 1990).  Therefore, a glacial interval was plotted during the late Capitanian (late Vyatian) within the Charbon Sub-Group based on the biostratigraphically diagnosed age of the laterally equivalent Bargo Claystone and Wilton Formation in the eastern Sydney Basin (Briggs 1998).  
 
Northeastern Sydney Basin

Dalwood Group: Lochinvar, Allandale, Rutherford, and Farley Formations
	The age of units within the early Permian Dalwood Group (Lochinvar, Allandale, Rutherford, and Farley Formations) found within the northeastern Sydney Basin, such as the Hunter Valley, is based on brachiopod biostratigraphic zonation (Briggs 1998).  The early Sakmarian Lochinvar Formation ranges from the base of the S. concentrica zone through a portion of the S. subcircularis zone.  It also contains palynomorphs from zone APP2.1 (formerly 3a and Granulatisporites confluens zones) (Roberts et al. 1995b).  Because the Cranky Corner area is a structural outlier of the Sydney Basin, the units in each area should correlate and differ only in their assigned nomenclature.  We infer the top of the Lochinvar Formation to be stratigraphically equivalent to the top of the Beckers Formation in the Cranky Corner region.  According to Booker (1961), the Lochinvar contains glacial erratics throughout the formation.  Therefore the formation is considered to be glacially-influenced, although its exact time range is unclear.  The Allandale Formation contains brachiopods from the S. subcircularis brachiopod assemblage and is likely stratigraphically equivalent to the Cranky Corner Sandstone (Briggs 1998).  The Allandale Formation contains outsized clasts in the lower half of the formation (Booker 1961).  Therefore, the age of the glacial interval is restricted to the lower half of the formation (Sterlitimakian) by assuming a linear sedimentation rate.  Based on biostratigraphic data, the Rutherford Formation spans the B. walkomi and T. strzeleckii brachiopod zones, while the Farley Formation ranges from E. curtosa through E. warwicki zones (Briggs 1998).  We infer these two formations to be stratigraphically equivalent to the Billy Brook Formation from the Cranky Corner region.  The basal portion of the Rutherford Formation is interpreted to have been glacially-influenced, base on the presence of outsized clasts and glendonites at the base of the formation (Booker 1961).  The Farley Formation contains outsized clasts in siltstone in the base of the formation which gradually become absent in the top part of the formation (Booker 1961).  Therefore, the lower half of the formation is considered glacially-influenced.  The stratigraphic scheme for the Dalwood Group is further supported by Mayne et al. (1974).

Greta Coal Measures & Maitland Group: Branxton Formation, Muree Sandstone & Mulbring Siltstone  
	The late Artinskian to early Kungurian age of the Greta Coal Measures and the late Kungurian to Roadian age of the overlying Maitland Group is discussed in the earlier “Cranky Corner” stratigraphy section.  Additionally, the Branxton Formation contains brachiopods from the E. maxwelli, E. davidi, and E. discinia biozones (Briggs 1998; Boyd & Leckie 2000).  The age of Muree Sandstone and overlying Mulbring Siltstone is taken from the biostratigraphic zonation of Briggs (1998).  The Muree Sandstone contains glacial facies throughout, while the Mulbring Siltstone contains outsized clasts that are restricted to the lower half of the formation.  Roberts et al. (1996) report a U-Pb SHRIMP date of 264.1 +/- 2.2 Ma on a volcanic member within the Mulbring Siltstone using the SL13 standard.  Even when this age is corrected to the TEMORA standard (266.7 Ma), it is younger than the biostratigraphic data suggests for the formation.  Because the biostratigraphic and radiometric data cannot be reconciled, the biostratigraphic data were preferred, particularly given reasonable lithostratigraphic correlations with other units throughout the basin.  This scheme is further supported by Mayne et al. (1974).

Tomago & Newcastle Coal Measures  
The Wordian through Changhsingian age of the Tomago and Newcastle Coal Measures is taken from Briggs (1998) and Mayne et al. (1974), based on palynological data and lithostratigraphic/ coal seam correlation.  The Tomago Coal Measures contain outsized clasts in the upper half of the formation, in the Dempsey and Shortland Formations, but not in the overlying Waratah Sandstone (Diessel 1992).  The Shortland Formation is equivalent to the Bargo Claystone (see “SE Sydney Basin”) (Diessel 1992). By assuming a linear sedimentation rate and applying the lithostratigraphic correlations with the southeastern Sydney Basin, the late Capitanian to earliest Wuchiapingian part of the Tomago Coal Measures is considered to be glacially-influenced.  
	
Southwestern Sydney Basin

Clyde Coal Measures, Shoalhaven Group: Yadboro/Tallong Conglomerates, Yarrunga Coal Measures, Snapper Point Formation, Wandrawandian Siltstone, Nowra Sandstone & Berry Siltstone, & Illawarra Coal Measures: Nile, Cullen-Bullen, Charbon & Wallerawang Sub-Groups
	The age of the Clyde Coal Measures and units within the overlying marine Shoalhaven group (Yadboro/Tallong Conglomerates, Yarrunga Coal Measures, Snapper Point Formaiton, Wandrawandian Siltstone, Nowra Sandstone, and Berry Siltstone) is taken from Briggs (1998), which is based on palynological data and lithostratigraphic correlation for the Clyde Coal Measures, and brachiopod data for the Shoalhaven Group (Herbert 1981; Tye et al. 1996; Briggs 1998).  This scheme is further supported by biostratigraphic work of Dickins et al. (1969).  The Clyde Coal Measures contain lower stage 3 (or APP2.1) microflora (Herbert 1981).  Upon core examination (DM Callala DDH1), approximately the basal half of the Yadboro/Tallong Conglomerates is composed of diamictite.  By assuming a linear sedimentation rate for the Yadboro/Tallong Conglomerates and the Yarrunga Coal Measures, the late Sakmarian to early Artinskian (Sterlitimakian to mid-Aktastinian) is thought to record an interval of glacially-influenced deposition.  The Wandrawandian Siltstone, Nowra Sandstone, Berry Siltstone, and Broughton Formation all contain glacial facies throughout the formations.  The stratigraphy of the units contained within the Illawarra Coal Measures in the Western Coalfield are discussed above (“Northwestern Sydney Basin”).  

Southeastern Sydney Basin

Wasp Head Formation & Shoalhaven Group: Pebbley Beach Formation, Snapper Point Formation, Wandrawandian Siltstone, Nowra Sandstone, Berry Siltstone & Broughton Formation
	The stratigraphy of the fully marine Wasp Head Formation and Shoalhaven Group in the southeastern Sydney Basin (Pebbley Beach Formation, Snapper Point Formation, Wandrawandian Siltstone, Nowra Sandstone, Berry Siltstone, Broughton Formation) is taken directly from Briggs (1998), which is based on available biostratigraphic data from these formations.  The age of the Wasp Head Formation is further supported by the palynological correlations of Archbold (2003).  Roughly, the lower half of the Wasp Head Formation contains evidence of glaciation with gradual climatic amelioration in the top half of the formation (Rygel et al. in revision).  This stratigraphic glacial trend was plotted relative to time assuming a linear sedimentation rate for the formation.  Lithostratigraphic correlations by Tye et al. (1996) demonstrate a diachronous contact between the Pebbley Beach Formation and the overlying Snapper Point Formation.  The lower Pebbley Beach Formation contains direct evidence of glaciation, while the upper Pebbley Beach Formation exhibits indirect evidence of glaciation in the form of large-scale relative sea level shifts interpreted to record a glacio-eustatic signal from distant glaciation (Fielding et al. 2006).  The Wandrawandian Siltstone, Nowra Sandstone, Berry Siltstone, and Broughton Formation all contain glacial facies throughout the formations.

Illawarra Coal Measures:  Pheasant’s Nest, Erins Vale, Wilton Formations, Bargo Claystone, Darkes Forest Sandstone, Allans Creek Formation, Kembla Sandstone & Eckersley Formation  
The stratigraphy of units within the Illawarra Coal Measures in the southeastern coastal exposures of the Sydney Basin, such as the Pheasant’s Nest Formation, Erins Vale Formation, Wilton Formation, Bargo Claystone, Darkes Forest Sandstone, Allans Creek Formation, Kembla Sandstone, and Eckersley Formation, are constrained from available brachiopod and palynological data of Briggs (1998).  The Erins Vale Formation and upper Wilton Formation contain evidence of glacial influence in the form of outsized clasts.  The duration of the upper Wilton Formation was estimated by assuming a linear sedimentation rate and converting the thickness and stratigraphic position of the glacially-influenced strata to time, placing a glacial interval in the early to late Capitanian.

References 

APAK, S.N., STUART, W.J., LEMON, N.M. & WOOD, G. 1997. Structural evolution of the Permian-Triassic Cooper Basin, Australia; relation to hydrocarbon trap styles. American Association of Petroleum Geologists Bulletin, 81, 533-555.
ARCHBOLD, N.W. 2003. Marine Early Permian (Asselian-Sakmarian) invertebrate Palaeontology of DM Tangorin DDH1, Cranky Corner Basin, New South Wales. In: Facer, R.A. & Foster, C.B., (eds) Geology of the Cranky Corner Basin, Coal and Petroleum Bulletin. 4, 155-166.
BALME, B.E. & FOSTER, C.B. 2003. Palynostratigraphy of the DM Tangorin DDH1, Cranky Corner Basin, New South Wales. In: Facer, R.A. & Foster, C.B., (eds) Geology of the Cranky Corner Basin, Coal and Petroleum Bulletin. 4, 127-154.
BLACK, L.P., KAMO, S.L., WILLIAMS, I.S., MUNDIL, R., DAVIS, D.W., KORSCH, R.J. & FOUDOULIS, C. 2003. The application of SHRIMP to Phanerozoic geochronology; a critical appraisal of four zircon standards. Chemical Geology, 200, 171-188.
BOOKER, F.W., 1961. Studies in Permian sedimentation in the Sydney Basin, New South Wales Department of Mines report.
BOYD, R. & LECKIE, D. 2000. Stratigraphy and correlation of the Greta Coal Measures. Advances in the Study of the Sydney Basin: Proceedings of the Symposium, 34, 61-70.
BRIGGS, D.J.C., 1998. Permian Productidina and Strophalosiidina from the Sydney-Bowen Basin and New England Orogen; systematics and biostratigraphic significance. Memoir of the Association of Australasian Palaeontologists, Association of Australasian Palaeontologists, Sydney, 19.
BRYAN, S.E., ALLEN, C.M., HOLCOMBE, R.J. & FIELDING, C.R. 2004. U-Pb zircon geochronology of Late Devonian to Early Carboniferous extension-related silicic volcanism in the northern New England Fold Belt. Australian Journal of Earth Sciences, 51, 645-664.
CLAOUE-LONG, J., COMPSTON, W., ROBERTS, J. & FANNING, C.M. 1995. Two Carboniferous ages: A comparison of SHRIMP zircon dating with conventional zircon ages and 40Ar/39Ar analysis. Geochronology Time Scales and Global Stratigraphic Correlation, SEPM Special Publication, 54, 3-21.
CLAOUE-LONG, J.C. & KORSCH, R.J. 2003. Numerical time measurement in the DM Tangorin DDH1 drillcore. In: Balme, B.E. & Foster, C.B., (eds) Geology of the Cranky Corner Basin, Coal and Petroleum Bulletin. 4, 179-206.
DEAR, J.F., MCKELLAR, R.G. & TUCKER, R.M., 1971. Geology of the Monto 1:250,000 sheet area. Brisbane, Queensland Department of Mines Report, 46.
DICKINS, J.M., GOSTIN, V.A. & RUNNEGAR, B. 1969. The age of the Permian sequence in the southern part of the Sydney Basin. In: Campbell, K.S.W., (ed) Stratigraphy and palaeontology; essays in honour of Dorothy Hill. Australian National University Press, Canberra, 211-225.
DIESSEL, C.F.K., 1992. Coal Bearing Depositional Systems, Springer-Verlag, Berlin, 362-363.
DRAPER, J.J., PALMIERI, V., PRICE, P.L., BRIGGS, D.J.C. & PARFREY, S.M. 1990. A biostratigraphic framework for the Bowen Basin. Bowen Basin Symposium 1990 Proceedings, 26-35.
DUNHULTY, J.A. & PACKHAM, G.H. 1962. Notes on the Permian sediments in the Mudgee District, New South Wales. Journal and Proceedings of the Royal Society of New South Wales, 95, 161-166.
EVANS, P.R. 1967. Upper Carboniferous and Permian palynological stages and their distribution in Eastern Australia. Record of the Bureau of Mineral Resources, Geology and Geophysics, Australia, 1967/99, 1-13 (unpubl.).
FIELDING, C.R., BANN, K.L., MACEACHERN, J.A., TYE, S.C. & JONES, B.G. 2006. Cyclicity in the nearshore marine to coastal, Lower Permian, Pebbley Beach Formation, southern Sydney Basin, Australia; a record of relative sea-level fluctuations at the close of the late Palaeozoic Gondwanan ice age. Sedimentology, 53, 453-463.
FIELDING, C.R., STEPHENS, C.J. & HOLCOMBE, R.J. 1997. Permian stratigraphy and paleogeography of the eastern Bown Basin, Gogango Overfolded Zone and Strathmuir Synclinorium in the Rockhampton-Mackay region of Central Queensland. In: Ashley, P.M. & Flood, P.G., (eds) Tectonics and Metallogenesis of the New England Orogen, Special Publication of the Geological Society of Australia. 19, 80-95.
FLOOD, P.G., MARX, W.T. & ROBERTS, C.L. 1993. Zeolite productions from the Escott Mine of Mount Gipps Limited, Werris Creek. Australasian mining and metallurgy; the Sir Maurice Mawby memorial volume, 19, 1431-1434.
GRADSTEIN, F.M., OGG, J.G. & SMITH, A.G., 2004. A Geologic Time Scale 2004, Cambridge University Press, Cambridge.
HAMILTON, D.S. 1993. Upper Watermark- Lower Black Jack/ Arkarula depositional episode. In: Tadros, N.Z., (ed) The Gunnedah Basin, New South Wales, Geological Survey of New South Wales Geology Memoir. 12, 213-244.
HECKEL, P.H. & GEOFFREY, C. 2006. Use of the new official names for the Subsystems, Series, and Stages of the Carboniferous system in international journals. Proceedings of the Geologists' Association, 117, 393-396.
HELBY, R.J. 1969. Preliminary palynological study of the Kuttung sediments in central eastern New South Wales. Record of the Geological Survey of New South Wales, 11, 5-14.
HERBERT, C. 1981. Late Palaeozoic glacigenic sediments of the southern Sydney Basin, New South Wales. In: Hambrey, M.J. & Harland, W.B., (eds) Earth's pre-Pleistocene glacial record. Cambridge University Press, Cambridge, 488-491.
HUTTON, A., BAMBERRY, W.J. & JONES, B.G. 1990. Southern and Western Coalfields of the Sydney Basin, Excursion Notes. 16-19 February, 1990, University of Wollongong, New South Wales.
JENKINS, T.B.H., CRANE, D.T. & MORY, A.J. 1993. Condont biostratigraphy of the Visean Series in eastern Australia. Alcheringa, 17, 211-283.
JONES, A.T., 2003. Sedimentological record of the late Paleozoic Gondwanan glaciation in Queensland. Ph.D. thesis, University of Queensland.
JONES, A.T. & FIELDING, C.R. 2004. Sedimentological record of the late Paleozoic glaciation in Queensland, Australia. Geology, 32, 153-156.
JONES, M.J. & TRUSWELL, E.M. 1992. Late Carboniferous and Early Permian palynostratigraphy of the Joe Joe Group, southern Galilee Basin, Queensland, and implications for Gondwanan stratigraphy. Bureau of Mineral Resources Geology and Geophysics Journal of Australian Geology and Geophysics, 13, 143-185.
KEMP, E.M., BALME, B.E., HELBY, R.J., KYLES, R.A., PLAYFORD, G. & PRICE, P.L. 1977. Carboniferous and Permian palynostratigraphy in Australia and Antactica: a review. Bureau of Mineral Resources, Geology, and Geophysics Journal of Australian Geology and Geophysics, 2, 177-208.
LEITCH, E.C., FERGUSSON, C.L., HENDERSON, R.A. & MORAND, V.J. 1994. Late Paleozoic arc flank and fore-arc basin sequence of the New England Fold Belt in the Stanage Bay region, central Queensland. Australian Journal of Earth Sciences, 41, 301-310.
LENNOX, P.G. & ROBERTS, J. 1988. The Hastings Block; a key to the tectonic development of the New England Orogen. In: Kleeman, J.D., (ed) New England Orogen; tectonics and metallogenesis. University of New England Department of Geology and Geophysics, Armidale, 68-77.
LINDSAY, J.F. 1966. Carboniferous subaqueous mass-movement in the Manning-Macleay Basin, Kempsey, New South Wales. Journal of Sedimentary Petrology, 36, 719-732.
MAYNE, S.J., NICHOLAS, E., BIGG-WITHER, A.L., RASIDI, J.S. & RAINE, M.J. 1974. Geology of the Sydney Basin; a review. Australian Bureau of Mineral Resources, Geology and Geophysics Bulletin, 149, 1-229.
MCELROY, C.T., BRANAGAN, D.F., RAAM, A. & CAMPBELL, K.S.W. 1969. Shoalhaven Group. In: Packham, G.H., (ed) Geology of New South Wales, Journal of the Geological Society of Australia. 16, part 1, 357-366.
MCKELLAR, J.L. 1977. Palynostratigraphy of core samples from the Hughenden 1:250 000 sheet area, northern Galilee and Eromanga basins. Queensland Government Mining Journal, 78, 393-399.
MCKELVEY, B.C. & MCPHIE, J. 1985. Tamworth Belt. In: Wagner, R.H., Winkler, P.C.F. & Granados, L.F., (eds) The Carboniferous of the World II: Australia, Indian subcontinent, South Africa, South America, and North Africa. Instituto Geologica y Minero de Espana and Empressa Nacional ADARO de Investigaciones Mineras, S.A., Madrid, 2, 15-23.
MENNING, M., WEYER, D., DROZDZEWSKI, G., VAN AMEROM, H.W.J. & WENDT, I. 1999. A Carboniferous time scale 2000; discussion and use of geological parameters as time indicators from Central and Western Europe. Geologisches Jahrbuch, A156, 3-44.
MORY, A.J. 1981. A review of early Carboniferous stratigraphy and correlations in the northern Tamworth Belt, New South Wales. Proceedings of the Royal Society of New South Wales, 105, 213-236.
NORVICK, M. 1974. Permian and Late Carboniferous palynostratigraphy of the Galilee Basin, Queensland. Australia Bureau of Mineral Resources, Geology and Geophysics Australia Record, 1974/141, 139.
OPDYKE, N.D., ROBERTS, J., CLAOUE-LONG, J., IRVING, E. & JONES, P.J. 2000. Base of the Kiaman; its definition and global stratigraphic significance. Geological Society of America Bulletin, 112, 1315-1341.
PLAYFORD, G. 1977. A lower Carboniferous palynoflora from the Drummond Basin, east-central Queensland. Proceedings of the Royal Society of Queensland, 88, 75-81.
PLAYFORD, G. 1978. Lower Carboniferous spores from the Ducabrook Formation, Drummond Basin, Queensland. Palaeontographica, 167B, 105-160.
PLAYFORD, G. 1985. Spores and Pollen. In: Wagner, R.H., Winkler, P.C.F. & Granados, L.F., (eds) The Carboniferous of the World II: Australia, Indian subcontinent, South Africa, South America, and North Africa. Instituto Geologica y Minero de Espana and Empressa Nacional ADARO de Investigaciones Mineras, S.A., Madrid, 2, 123-126.
PRICE, P.L., FILATOFF, J., WILLIAMS, A.J., PICKERING, S.A. & WOOD, G.R. 1985. Late Paleozoic and Mesozoic palynostratigraphical units. CSR Oil and Gas Division, Palynological Facility Report, 274/25.
ROBERTS, J. 1975. Early Carboniferous brachiopod zones of eastern Australia. Journal of the Geological Society of Australia, 22, 1-32.
ROBERTS, J. 1985. Hunter Region. In: Wagner, R.H., Winkler, P.C.F. & Granados, L.F., (eds) The Carboniferous of the World II: Australia, Indian subcontinent, South Africa, South America, and North Africa. Instituto Geologica y Minero de Espana and Empressa Nacional ADARO de Investigaciones Mineras, S.A., Madrid, 2, 23-33.
ROBERTS, J. unpubl. data. Tamworth Belt regional correlation carts.
ROBERTS, J., CLAOUE-LONG, J. & JONES, P.J. 1995a. Australian Early Carboniferous time. In: Kent, D.V., Aubry, M.P. & Hardenbol, J., (eds) Geochronology, time scales and global stratigraphic correlation. Society of Economic Petrologists and Mineralogists (SEPM) Special Publication, 54, 23-40.
ROBERTS, J., CLAOUE-LONG, J., JONES, P.J. & FOSTER, C.B. 1995b. SHRIMP zircon age control of Gondwanan sequences in the Late Carboniferous and Early Permian Australia. In: Dunay, R.E. & Hailwood, E.A., (eds) Non-biostratigraphical methods of dating and correlation. Special Publications. Geological Society of London, 89, 145-174.
ROBERTS, J., CLAOUE-LONG, J.C. & FOSTER, C.B. 1996. SHRIMP zircon dating of the Permian System of eastern Australia. Australian Journal of Earth Sciences, 43, 401-421.
ROBERTS, J., JONES, A.T. & JENKINS, B.H. 1993a. Revised correlations for Carboniferous marine invertebrate zones of eastern Australia. Alcheringa, 17, 353-376.
ROBERTS, J., LEITCH, E.C., LENNOX, P.G. & OFFLER, R. 1995c. Devonian-Carboniferous stratigraphy of the eastern Hastings Block, New England Orogen, eastern Australia. Australian Journal of Earth Sciences, 42, 609-634.
ROBERTS, J., LENNOX, P.G. & OFFLER, R. 1993b. The geological development of the Hastings Terrane- displaced fore-arc fragments of the Tamworth Belt. New England Orogen 1993 Conference Proceedings, 231-242.
ROBERTS, J., OFFLER, R. & FANNING, M. 2004. Upper Carboniferous to Lower Permian volcanic successions of the Carrol-Nandewar region, northern Tamworth Belt, southern New England Orogen, Australia. Australian Journal of Earth Sciences, 51, 205-232.
ROBERTS, J., OFFLER, R. & FANNING, M. 2006. Carboniferous to Lower Permian stratigraphy of the southern Tamworth Belt, southern New England Orogen, Australia: boundary sequences of the Werrie and Rouchel blocks. Australian Journal of Earth Sciences, 53, 249-284.
ROBERTS, J., WANG, X. & FANNING, M. 2003. Stratigraphy and correlation of Carboniferous ignimbrites, Rocky Creek region, Tamworth Belt, southern New England Orogen, New South Wales. Australian Journal of Earth Sciences, 50, 931-954.
RYGEL, M.C., FIELDING, C.R., BANN, K.L., FRANK, T.D., BIRGENHEIER, L. & TYE, S.C. in revision. The early Permian Wasp Head Formation, Sydney Basin: High-latitude shallow marine sedimentation following the late Asselian-early Sakmarian glacial event in eastern Australia. Sedimentology.
SUSSMILCH, C.A. & DAVID, T.W.E. 1919. Sequence, glaciation and correlation of the Carboniferous rocks of the Hunter River district, New South Wales. Journal and Proceedings of the Royal Society of New South Wales, 53, 246-338.
TADROS, N.Z. 1993. Lithostratigraphy. In: Tadros, N.Z., (ed) The Gunnedah Basin, New South Wales, Geological Survey of New South Wales Geology Memoir. 12, 95-133.
TRAPP, E., KAUFMANN, B., MEZGER, K., KORN, D. & WEYER, D. 2004. Numerical calibration of the Devonian-Carboniferous boundary; two new U-Pb isotope dilution-thermal ionization mass spectrometry single-zircon ages from Hasselbachtal (Sauerland, Germany). Geology, 32, 857-860.
TYE, S.C., FIELDING, C.R. & JONES, B.G. 1996. Stratigraphy and sedimentology of the Permian Talaterang and Shoalhaven groups in the southernmost Sydney Basin, New South Wales. Australian Journal of Earth Sciences, 43, 57-69.
WHETTEN, J.T. 1965. Carboniferous glacial rocks from the Werrie Basin, New South Wales, Australia. Geological Society of America Bulletin, 76, 43-56.

Figure Captions

Figure 1. Generalised, composite, graphic sedimentological logs of Carboniferous and Permian successions in key outcrop areas (see Fig. 2B of main paper for location map), showing distribution of evidence for glacial influence on sediment accumulation. Glacial interval codes are as in Figure 2A, main paper. A) Lake Galilee Sandstone and Jericho formation of Joe Joe Group in the Galilee Basin of central Queensland, showing correlation of discrete intervals containing evidence of glaciation, and separation of those intervals by sections containing no evidence for glacial influence. Column on left is a more detailed log of the Lake Galilee Sandstone in fully cored drillhole GSQ Jericho-2. Correlations are lithostratigraphic, but are supported by the palynostratigraphic biozonation of Jones & Truswell (1992), B) Permian succession in the Denison Trough of the western Bowen Basin, central Queensland, showing the distribution of mainly indirect evidence for glacial events, C) Carboniferous and Permian succession in the Rocky Creek syncline and overlying Gunnedah Basin, northern New South Wales, D) Carboniferous and Permian succession in the Gresford Block and adjacent northern Sydney Basin, central New South Wales, E) Permian succession in the southeastern Sydney Basin of southern New South Wales, and key to symbols used.