18 The FO for common Uvaesporites imperialis is based on occurrences from multiple localities. In the Sverdrup Basin it is recorded from near the base of the Blind Fiord Formation (Fisher 1979, Utting 1994), where records exist of the ammonoid Otoceras concavum, a taxon previously regarded as representing the base of the Triassic. However, with the recent designation of a GSSP at the base of the Triassic, the Otoceras concavum Zone is now within the uppermost Permian. In Svalbard, Uvaesporites imperialis has been recorded at various locations, including the Deltadalen and Festningen sections, where the ammonoid Otoceras boreale was also recorded (Mørk et al. 1999; Vigran et al. 2014). In both the Norwegian and Canadian Arctic, and in North East Greenland, Uvaesporites imperialis commonly occurs in tetrads. Abundant Uvaesporites imperialis is also recorded on the Finnmark Platform, Barents Sea, where two shallow stratigraphic cores provide detailed palynology (Mangerud 1994; Hochuli et al. 2010) across the Permian/Triassic boundary. Palynology that was linked to high-resolution carbon isotope curves across the boundary layers (Looy et al. 2001; Twitchett et al. 2001; Hermann et al. 2010; Hochuli et al. 2010) provides important understanding of the boundary interval and correlation to the global stratotype. Vigran et al. (2014) linked the base of abundant Uvaesporites imperialis to the very latest Permian (Changhsingian), although for practical purposes, this event is often related to the base of the Triassic.

19 The FO of common Uvaesporites imperialis is taken as the base of the ammonoid Otoceras concavum zone.

20 The FO of Reduviasporonites chalastus is based on multiple records from the Arctic, including the Sverdrup Basin, where Utting (1994) defined his oldest Triassic palynology zone based on this species (Utting used the name Tympanicysta stoschiana, now considered a taxonomic junior synonym of Reduviasporonites chalastus). Utting (1985, 1989) recorded the species from the Blind Fiord Formation. It has also been recorded from the Norwegian Arctic, including the Finnmark Platform, Barents Sea (Mangerud 1994; Hochuli et al. 2010) and Svalbard (Mørk et al. 1999; Vigran et al. 2014). Reduviasporonites chalastus is of probable algal origin (Foster et al. 2002; Hochuli 2016). For discussion of age, see also Uvaesporites imperialis.

21 The FO of Reduviasporonites chalastus is taken as the base of the ammonoid Otoceras concavum zone.

22 The FO of Lunatisporites noviaulensis is based on multiple records from the Arctic, including from the Blind Fiord and Bjorne formations in the Sverdrup Basin (Utting 1985, 1989, 1994). Lunatisporites noviaulensis has also been recorded from basal Triassic on the Finnmark Platform (Mangerud 1994), with the FO slightly above the base of the Uvaesporites imperialis acme.

23 The FO of Lunatisporites noviaulensis is taken as the base of the Griesbachian (equivalent to the Induan).

24 The FO of Ephedripites steevesii is based on multiple records from the Arctic, including the Sverdrup Basin (Utting 1985, 1989, 1994, from the Blind Fiord Formation) and Spitsbergen (Vigran et al. 2014). On the Finnmark Platform of the Barents Sea, one of us (NWP) has observed that this species appears abruptly in a short interval corresponding to the Permian/Triassic boundary carbon isotope excursion.

25 The FO of Ephedripites steevesii is here taken as the base of the Griesbachian (equivalent to the Induan).

26 In the Sverdrup Basin, Uvaesporites imperialis occurs in the Bjorne and Blind Fiord Formation, where the ammonoid Otoceras boreale is also recorded (Tozer 1967). In the Barents Sea, the LO of common Uvaesporites imperialis occurs close to the base of the Triassic according to Hermann et al. (2010). Mangerud (1994) also noted this event. The event is linked to high-resolution carbon-isotope curves across the boundary layers (Hermann et al. 2010; Hochuli et al. 2010), providing correlation to the global stratotype and indicating a LO of common Uvaesporites imperialis at about 20–30 ka above its FO, which is at the base of the ammonoid Otoceras concavum Zone. In Svalbard the event is recorded at various locations, including the Deltadalen section, where the ammonoid Otoceras boreale was also recorded (Mørk et al. 1999; Vigran et al. 2014). In both the Norwegian and Canadian Arctic, Uvaesporites imperialis commonly occurs in tetrads (e.g., Mangerud 1994; Hochuli et al. 2017; GM, personal observations).

27 The LO of common Uvaesporites imperialis is here taken as 5% above the base of the Griesbachian (equivalent to the base of the Induan).

28 The FO of consistent Proprisporites pocockii is based on multiple records from the Arctic, including those from the Sverdrup Basin (Utting 1985, from the Bjorne Formation). It has been also recorded from the Finnmark Platform of the Barents Sea (Mangerud 1994), and from the Vardebuka Formation on Svalbard (Mangerud and Konieczny 1993; Mørk et al. 1999). Based on multiple datasets, Vigran et al. (2014) used this species to define their Proprisporites pocockii Composite Assemblage Zone. This zone correlates to similar assemblages in the Svalis Dome (Vigran et al. 1998), where records occur of the ammonoid Ophiceras, which is assigned to the ammonoid Ophiceras commune Zone of late Griesbachian age.

29 The FO of consistent Proprisporites pocockii is here taken as the base of the ammonoid Ophiceras commune zone.

30 The FO of consistent Aratrisporites is based on multiple records from the Norwegian Arctic. Based on several datasets, Vigran et al. (2014) placed the FO of this event at the base of their Proprisporites pocockii Composite Assemblage Zone, which correlates to similar assemblages in the Svalis Dome (Vigran et al. 1998). At the latter locality, records occur of the ammonoid Ophiceras, which is assigned to the ammonoid Ophiceras commune Zone of late Griesbachian age. In East Greenland Schneebeli-Hermann et al. (2017) recorded Aratrisporites in the Griesbachian succession.

31 The FO of consistent Aratrisporites is is here taken as the base of the ammonoid Ophiceras commune Zone.

32 The LO of Vittatina occurs near the top of the Griesbachian Substage. Vittatina is regarded as a typical Permian taxon, fading out gradually above the Permian/ Triassic boundary, although there has been debate as to whether Triassic records represent reworking (e.g., Hochuli et al. 1989; Mangerud 1994; Utting et al. 2004; Vigran et al. 2014). Vigran et al. (2014) concluded that Vittatina ranges sporadically up to the top of their Proprisporites pocockii Composite Assemblage Zone. The assemblage characterizing this zone correlates with similar assemblages in the Svalis Dome (Vigran et al. 1998), where records occur of the ammonoid Ophiceras, which is assigned to the ammonoid Ophiceras commune Zone of late Griesbachian age. The LO of Vittatina is also recorded further south: in East Greenland, Schneebeli-Hermann et al. (2017) recorded Vittatina ranging into the Dienerian.

33 The LO of Vittatina is taken as 70% up from the base of the Griesbachian (equivalent to the base of the Induan).

34 The FO of common Densoisporites nejburgii is based on multiple records from the Arctic, including those from the Sverdrup Basin (Fisher 1979) and from the Norwegian Arctic (Vigran et al. 2014).

35 The FO of common Densoisporites nejburgii is taken here as the base of the Boreal ammonoid Vavilovites sverdrupi Zone.

36 The FO of consistent Maculatasporites is based on multiple records from the Norwegian Arctic. It defines the base of the Maculatasporites Composite Assemblage Zone of Vigran et al. (2014), who correlated assemblages from the Svalis Dome containing Maculatasporites spp. to similar assemblages from Bjørnøya (Mørk et al. 1990); at the latter locality, Dienerian ammonoids of the ammonoid Vavilovites sverdrupi Zone were recorded from the Urd Formation. The early Induan is dominated by taeniate bisaccates, but there seems generally to be a major turnover in the Dienerian, continuing in the Smithian.

37 The FO of consistent Maculatasporites is taken here as the base of the Boreal ammonoid Vavilovites sverdrupi Zone.

38 The LO of common Cycadopites and Pretricolpipollenites is based on multiple records from the Norwegian Arctic. Their LOs corresponds with the top of the Maculatasporites Composite Assemblage Zone of Vigran et al. (2014), who correlated assemblages with these taxa to similar assemblages from Bjørnøya (Mørk et al. 1990), where ammonoids of the Vavilovites sverdrupi Zone of Dienerian age were recorded from the Urd Formation. Hochuli et al. (1989) also mentions a distinctive palynoflora with common Cycadopites and Pretricolpipollenites from a sample dated Dienerian by ammonoids in the Bertilryggen section on Spitsbergen.

39 The LOs of common Cycadopites and Pretricolpipollenites are taken as the base of the Smithian (lower Olenekian).

40 The FO of common to abundant Punctatisporites fungosus is based on multiple records from the Norwegian Arctic. It has been recorded by Vigran et al. (2014) and Rossi et al. (2019) from the base of the Naumovaspora striata Composite Assemblage Zone from several surface sections and wells. The zone is dated by its co-occurrence with the ammonoid Wasachites tardus from the Svalis Dome (Vigran et al. 1998, 2014); however, a gap occurs in the coring between this core and the underlying core, so the FO could be somewhat older. Common Punctatisporites fungosus has also been recorded in assemblages from beds with the early Olenekian (Smithian) ammonoid Eufleminigites romunderi at Vikinghøgda (Mørk et al. 1999), from Peary Land, North-East Greenland (Lindström et al. 2020) and at Bjørnøya (Mørk et al. 1990); at that locality, ammonoids were recorded from the middle parts of the Urd Formation. Similarly, in the Russian Barents Sea, the FO of Punctatisporites fungosus is recorded in the Smithian T₁O₁ palynocomplex (Mørk et al. 1993; Fefilova 2013a).

41 The FO base of common to abundant Punctatisporites fungosus is taken here as the base of the Boreal ammonoid Euflemingites romunderi Zone.

42 The LO of sporadic Proprisporites pocockii is based on data from Vigran et al. (1998, 2014), who recorded infrequent occurrences of this species ranging up to the middle of their Naumovaspora striata Composite Assemblage Zone. The assemblage comprising the latter zone was recorded in beds where the ammonoid Wasatchites tardus Zone was defined in the Svalis Dome. On Bjørnøya, Proprisporites pocockii occurs sporadically in the Urd Formation (Mørk et al. 1990).

43 The LO of sporadic Proprisporites pocockii is taken as 50% up from the base of the ammonoid Wasatchites tardus Zone.

44 The LO of sporadic Naumovaspora striata is based on multiple records from the Norwegian Arctic. The LO of Naumovaspora striata defines the top of the Naumovaspora striata Assemblage Zone (Vigran et al. 2014), which has been recorded in multiple localities. In the reference section for this zone (a core at the Svalis Dome in the Barents Sea), the latest Olenekian (late Smithian) ammonoid index taxon Wasachites tardus was recorded. A similar assemblage was also documented on Bjørnøya, from beds with the slightly older ammonoid Euflemingites romunderi (Mørk et al. 1990).

45 The LO of sporadic Naumovaspora striata is taken here as the base of the Spathian (upper Olenekian).

46 The LO of common to abundant Punctatisporites fungosus is based on multiple records from the Norwegian Arctic. It partly defines the base of the Naumovaspora striata Assemblage Zone of Vigran et al. (2014), which was recorded from a core from Svalis Dome. Vigran et al. dated this zone as Smithian based on records of the ammonoid Wasachites tardus. In wells from the Barents Sea, this event corresponds to the transition between the Havert and Klappmyss formations (Rossi et al. 2019). A similar assemblage was recorded at Bjørnøya, from beds containing the ammonoid Euflemingites romunderi (Mørk et al. 1990).

47 The LO of common Punctatisporites fungosus is taken here as the base of the Spathian (upper Olenekian).

48 The FO of common Pechorosporites disertus is based on multiple records from the Norwegian Arctic. Its FO defines the base of the Pechorosporites disertus Assemblage Zone according to Vigran et al. (2014), dated as early Spathian. However, little faunal evidence exists for the age of this zone, as it occurs between ammonoid-dated Smithian and late Spathian sections in the Svalis Dome.

49 The FO of common Pechorosporites disertus is taken here as the base of the Spathian (upper Olenekian).

50 The LO of common Pechorosporites disertus is based on multiple records from the Norwegian Arctic. Its LO defines the top of the Pechorosporites disertus Assemblage Zone (Vigran et al. 1998, 2014) and has been recorded in the upper-most Klappmyss Formation, where it has been assigned an early Spathian age. However, little faunal evidence exists for the age of this zone, as it occurs between ammonoid-dated Smithian and late Spathian sections. The appearance of the taxon in the Russian Barents Sea seem to be slightly earlier, with occurrences reported in the Dienerian T1i2 palyno-complex (Fefilova 2013a, b).

51 The LO of common Pechorosporites disertus is taken here as the base of the ammonoid Keyserlingites subrobustus Zone.

52 The FO of Jerseyiaspora punctispinosa is based on multiple records from the Norwegian Arctic. It was reported by Mangerud and Rømuld (1991) from the Svalis Dome, in beds with the ammonoid Keyserlingites subrobustus. It has also been recorded in various localities in Svalbard, including the type section of the Vikinghøgda Formation (from the upper part of the Vendomdalen Member; Mørk et al. 1999), and from several exploration wells (Vigran et al. 2014; Paterson and Mangerud 2017; Rossi et al. 2019). The FO of Jerseyiaspora punctispinosa defines the base of the Jerseyiaspora punctispinosa Composite Assemblage Zone (Vigran et al. 2014).

53 The FO of Jerseyiaspora punctispinosa is taken here as the base of the late Spathian Boreal ammonoid Keyserlingites subrobustus Zone.

54 The FO of Protodiploxypinus is based on multiple records from the Norwegian Arctic. Mangerud and Rømuld (1991) reported its FO from the Svalis Dome, in beds containing the ammonoid Keyserlingites subrobustus. The FO of Protodiploxypinus also partly defines the base of the Jerseyiaspora punctispinosa Composite Assemblage Zone (Vigran et al. 2014).

55 The FO of Protodiploxypinus is taken here as the base of the Boreal ammonoid Keyserlingites subrobustus Zone.

56 The FO of Cyclotriletes oligogranifer is based on multiple records from the Norwegian Arctic. It was reported by Mangerud and Rømuld (1991) from the Svalis Dome, with its LO in beds with the late Spathian ammonoid Keyserlingites subrobustus. It has also been recorded in various localities in Svalbard (Vigran et al. 2014), appearing approximately at the same time as other species of Cyclotriletes such as Cyclotriletes pustulatus.

57 The FO of Cyclotriletes oligogranifer is taken here as the base of the Boreal ammonoid Keyserlingites subrobustus Zone.

58 The FO of sporadic Striatella seebergensis is based on multiple records from the Arctic, including the Sverdrup Basin (Fisher 1979). In the Norwegian Arctic it was reported by Mangerud and Rømuld (1991) from the Svalis Dome, in beds with the late Spathian ammonoid Keyserlingites subrobustus. It has also been recorded from various localities in Svalbard, including the type-section of the Vikinghøgda Formation (from the upper part of the Vendomdalen Member; Mørk et al. 1999), and from several exploration wells (Vigran et al. 2014; Rossi et al. 2019). Its FO partly defines the base of the Jerseyiaspora punctispinosa Composite Assemblage Zone (Vigran et al. 2014).

59 The FO of sporadic Striatella seebergensis is taken here as the base of the Boreal ammonoid Keyserlingites subrobustus Zone.

60 The FO of consistent Carnisporites spiniger is based on multiple records from the Norwegian Arctic. Mangerud and Rømuld (1991) and Vigran et al. (1998) recorded its consistent FO from the Steinkobbe Formation at the Svalis Dome, from a core with the ammonoid Karangatites evolutus, which is dated as early Anisian. Vigran et al. (2014) defined the Carnisporites spiniger Composite Assemblage Zone (called Anapiculatisporites spiniger Assemblage Zone therein) based on the FO of consistent Carnisporites spiniger. Its FO has been also recorded from a shallow core in the Sentralbanken area, together with ammonoids of the Lenotropis caurus Zone (Vigran et al. 2014), demonstrating that it ranges up into the Anisian. The LO Carnisporites spiniger was also noted by Paterson and Mangerud (2017) in the lower Kobbe Formation from the Nordkapp Basin, southern Barents Sea.

61 The FO of consistent Carnisporites spiniger is taken here as the base of the Boreal ammonoid Karangatites evolutus Zone.

62 The FO of consistent Illinites chitonoides is based on multiple records from the Norwegian Arctic. Mangerud and Rømuld (1991) and Vigran et al. (1998) recorded its FO from the Svalis Dome, from a core with the ammonoid Karangatites evolutus, which is regarded as early Anisian. Vigran et al. (2014) also noted that its consistent FO corresponds with the base of their Carnisporites spiniger Composite Assemblage Zone (called Anapiculatisporites spiniger Assemblage Zone therein).

63 The FO of consistent Illinites chitonoides is taken here as the base of the Boreal ammonoid Karangatites evolutus Zone.

64 Mangerud and Rømuld (1991) and Vigran et al. (1998) recorded the FO of consistent (and in some intervals common) Cordaitina gunyalensis from the middle part of the middle Anisian ammonoid Anagymnotoceras varium Zone in the Svalis Dome. However, Vigran et al. (2014) reported a considerably older FO for the taxon, at the base of their early Spathian Pechosporites disertus Composite Assemblage Zone (Vigran et al. 2014, fig 3b), indicating some uncertainty as to its FO. This distinct monosaccate pollen is a good index species; but because of its large size (often around 200 µm) it may not always survive routine palynological laboratory procedures intact and is often recorded as specimens with a missing corpus.

65 The FO of consistent Cordaitina gunyalensis is taken here as the base of the Anisian.

66 The FO of consistent Dyupetalum vicentinense is based on multiple records from the Norwegian Arctic. Although rare, the species has been recorded from many localities and is a characteristic element of the Triadispora obscura Composite Assemblage Zone (Vigran et al. 2014). This zone has been found in in association with the ammonoid Anagymnotoceras varium in the Svalis Dome, Barents Sea (Mangerud and Rømuld 1991). Hochuli et al. (1989) recorded this species with a lowest occurrence at or near the base of their Assemblage K, dated as late Anisian; however, it was later recorded in older sections dated by ammonoids. A single occurrence of Dyupetalum vicentinense was also noted in the Klappmyss Formation, from shallow-core material from the Barents Sea, in association with the late Spathian Jerseyiaspora punctispinosa Composite Assemblage Zone (Vigran et al. 2014, p. 145).

67 The FO of consistent Dyupetalum vicentinense is taken here as the base of the middle Anisian Boreal ammonoid Anagymnotoceras varium Zone.

68 The LO of consistent Densoisporites nejburgii is based on multiple records from the Norwegian Arctic. Hochuli et al. (1989) noted that its first downhole occurrence was around the top of the middle Anisian (their Assemblage L). In the Barents Sea, Mangerud and Rømuld (1991) recorded its youngest occurrence in the middle of their Anagymnotoceras varium ammonoid Zone in the Svalis Dome. Vigran et al. (2014) noted its LO within their Carnisporites spiniger Composite Assemblage Zone (called Anapiculatisporites spiniger Assemblage Zone therein) of early Anisian age.

69 The LO of Densoisporites nejburgii is taken here as 50% up from the base of the ammonoid Anagymnotoceras varium Zone.

70 The LO of consistent Jerseyiaspora punctispinosa is based on multiple records from the Norwegian Arctic. In the Barents Sea, Mangerud and Rømuld (1991) and Vigran et al. (1998) recorded its consistent occurrence in the Svalis Dome from a core with the ammonoid Anagymnotoceras varium, corresponding to the top of the middle Anisian. Only one occurrence is recorded in a younger core at the same location, probably representing reworking. Vigran et al. (2014) also recorded it as common from exploration wells and defined its LO as the top of their Triadispora obscura Composite Assemblage Zone, an observation supported also by records from Hochuli et al. (1989). From the southern Barents Sea, Paterson and Mangerud (2017) noted the LO of consistent Jerseyiaspora punctispinosa in the middle part of the Kobbe Formation. Somewhat younger occurrences of Jerseyiaspora punctispinosa in the Ladinian Echinitosporites iliacoides and Carnian Aulisporites astigmosus Composite Assemblage Zone were interpreted by Vigran et al. (2014, p. 130, 149) as reworking.

71 The LO of consistent Jerseyiaspora punctispinosa is taken here as 50% up from the base of the Anisian.

72 The FO of consistent to common Chasmatosporites is based on multiple records from the Norwegian Arctic. This taxon was recorded from the base of the Protodiploxypinus decus Composite Assemblage Zone of Vigran et al. (2014) with ammonoids of the Frechites laqueatus Zone, which is regarded as late Anisian (Vigran et al. 1998). Mueller et al. (2016) reported consistent Chasmatosporites from the base of the Tschermakfjellet Formation on Spitsbergen, which they assigned to the Julian (lower Carnian).

73 The FO of consistent to common Chasmatosporites is taken here as the base of the late Anisian ammonoid Frechites laqueatus Zone.

74 The FO of Protodiploxypinus decus is based on multiple records from the Norwegian Arctic. In the Barents Sea, it was recorded from the upper part of the Steinkobbe Formation in the Svalis Dome by Vigran et al. (1998). Its FO was used to define the Protodiploxypinus decus Composite Assemblage Zone of Vigran et al. (2014) and was calibrated to the upper Anisian ammonoid Frechites laqueatus in the same core. Note that Vigran et al. (2014, p. 71) erroneously stated that the LO (rather than FO) of Protodiploxypinus decus is in this ammonoid zone. Those authors also reported rare occurrences of Protodiploxypinus decus in the early Anisian Anapiculatisporites spiniger Composite Assemblage Zone, but these are likely misidentified.

75 The FO of Protodiploxypinus decus is taken here as the base of the ammonoid Frechites laqueatus Zone.

76 The FO of consistent Protodiploxypinus ornatus is based on multiple records from the Norwegian Arctic. Its FO corresponds to the base of Protodiploxypinus decus Composite Assemblage Zone of Vigran et al. (2014), which is calibrated to ammonoid records of the Frechites laqueatus Zone, of late Anisian age. Note that Vigran et al. 2014 (p. 71) erroneously stated that the LO (rather than the FO) of Protodiploxypinus ornatus is in this ammonoid zone.

77 The FO of consistent Protodiploxypinus ornatus is taken here as the base of the ammonoid Frechites laqueatus Zone.

78 The FO of Echinitosporites iliacoides is based on multiple records from the Norwegian Arctic. Its base defines the base of the Echinitosporites iliacoides Composite Assemblage Zone of Vigran et al. (2014), which was established at the base of the Ladinian Stage. This event is constrained by late Anisian ammonoid dating just below. Echinitosporites iliacoides is not very common but is a very distinctive marker species. It is reported from several locations in the Barents Sea (Hochuli et al. 1989; Mørk et al. 1990; Bugge et al. 2002a; Vigran et al. 1998, 2014; Paterson and Mangerud 2017, 2019; Paterson et al. 2018) and from Svalbard (Mørk et al. 1990, 1999); despite its small size and relatively rare occurrence, it is an important marker.

79 The FO of Echinitosporites iliacoides is taken here as the base of the Ladinian.

80 The FO of consistent Schizaeoisporites worsleyi is based on multiple records in the Norwegian Arctic. It was first described by Bjærke and Manum (1977) from Hopen Island. Vigran et al. (1998) recorded it in three Ladinian cores in the Svalis Dome, Barents Sea. No independent faunal evidence exists from the three Ladinian cores in the Svalis Dome, but the cored succession overlies upper Anisian successions dated by ammonoids. The range base of Schizaeoisporites worsleyi corresponds approximately to the base of the Echinitosporites iliacoides Composite Assemblage Zone of Vigran et al. (2014), which is set at the base of the Ladinian Stage. Similarly, in the Russian Barents Sea, Schizaeoisporites worsleyi has an FO in the Ladinian T₂l Zone (Mørk et al. 1993). A single occurrence of this taxon has been reported from the middle Anisian Triadispora obscura Composite Assemblage Zone from central Spitsbergen (Vigran et al. 2014, p. 98). In the Barents Sea, a few records of Schizaeoisporites worsleyi extend down to the early Anisian Anapiculatisporites spiniger Composite Assemblage Zone (Vigran et al. 2014, p. 189).

81 The FO of consistent Schizaeoisporites worsleyi is here taken as the base of the Ladinian.

82 The FO of consistent Triadispora verrucata is based on multiple records from the Norwegian Arctic (e.g., Hochuli et al. 1989; Vigran et al. 1998; Paterson and Mangerud 2017). Its base corresponds approximately to the base of the Echinitosporites iliacoides Composite Assemblage Zone of Vigran et al. (2014), which is correlated with the base of the Ladinian Stage. On central Spitsbergen, rare occurrences of Triadispora verrucata are known from the late Anisian Protodiploxypinus decus Composite Assemblage Zone (Vigran et al. 2014, p. 98). Similarly, Paterson and Mangerud (2017) recorded specimens of Triadispora verrucata from the middle Anisian Triadispora obscura Composite Assemblage in exploration wells from the southern Barents Sea.

83 The FO of consistent Triadispora verrucata is taken here as the base of the Ladinian.

84 The FO of Ovalipollis pseudoalatus is based on multiple records from the Norwegian Arctic. The species was recorded in all three Ladinian cores in the Svalis Dome, Barents Sea (Vigran et al. 1998). Its base corresponds approximately to the base of the Echinitosporites iliacoides Composite Assemblage Zone of Vigran et al. (2014), the base of which is set at the base of the Ladinian. An FO of Ovalipollis pseudoalatus at the base Ladinian was also reported by Hochuli et al. (1989).

85 The FO of Ovalipollis pseudoalatus is taken here as the base of the Ladinian.

86 The FO of consistent Staurosaccites quadrifidus is based on multiple records from the Norwegian Arctic. The species was recorded in all three Ladinian cores in the Svalis Dome, Barents Sea (Vigran et al. 1998). Its base corresponds approximately to the base of the Echinitosporites iliacoides Composite Assemblage Zone of Vigran et al. (2014), which is set at the base of the Ladinian. We note that rare older occurrences of Staurosaccites quadrifidus have been reported from assemblages assigned to the early Anisian Anapiculatisporites spiniger Composite Assemblage Zone, for example from western Spitsbergen and Barentsøya (Vigran et al. 2014). Elsewhere, Paterson and Mangerud (2017) recorded rare specimens of Staurosaccites quadrifidus from the late Anisian Protodiploxypinus decus Composite Assemblage Zone in exploration wells from the southern Barents Sea.

87 The FO of consistent Staurosaccites quadrifidus is taken here as the base of the Ladinian.

88 The FO of common to abundant Semiretisporis hochulii is based on multiple records from the Norwegian Arctic. The taxon has variously been reported informally in the literature as Semiretisporis “barentszi” (van Veen 1985), Semiretisporis sp. A (Vigran et al. 1998, pl. 9, fig. 2), Semiretisporis sp. 1 (Hounslow et al. 2008, fig. 7) and Semiretisporis sp. A (“barentzii”) (Vigran et al. 2014). The species was formally described as Semiretisporis hochulii by Paterson and Mangerud (2019). Vigran et al. (1998) recorded it from the base of their oldest Ladinian core at the Svalis Dome, Barents Sea, co-occurring with Echinitosporites iliacoides. Paterson et al. (2018) recorded common Semiretisporis hochulii from the lower part of the De Geerdalen Formation at Sentralbanken.

89 The FO of common to abundant Semiretisporis hochulii is taken here as the base of the Ladinian.

90 The FO of sporadic Enzonalasporites vigens is based on multiple records from the Norwegian Arctic, including several localities on Svalbard (Vigran et al. 2014). Hochuli et al. (1989) also reported Enzonalasporites vigens in their early Carnian Assemblage “F”. Vigran et al. (2014) reported the FO of Enzonalasporites vigens from the base of their Aulisporites astigmosus Composite Assemblage Zone, corresponding to the base of the Carnian. While most typical of the early Carnian succession, rare occurrences of the taxon have been recorded in assemblages assigned to the Ladinian Echitosporites iliacoides Composite Assemblage Zone from Spitsbergen and the Barents Sea (Vigran et al. 2014).

91 The FO of Enzonalasporites vigens is taken here as the base of the Carnian.

92 The FO of sporadic Camerosporites secatus is based on multiple records from the Norwegian Arctic. Vigran et al. (2014) recorded the species from the base of their Aulisporites astigmosus Composite Assemblage Zone, corresponding to the base of the Carnian Stage.

93 The FO of Camerosporites secatus is taken here as the base of the Carnian.

94 The FO of consistent Aulisporites astigmosus is based on multiple records from the Norwegian Arctic. Vigran et al. (2014) recorded the species from the base of their Aulisporites astigmosus Composite Assemblage Zone, corresponding to the base of the Carnian. Hochuli et al. (1989) also reported Aulisporites astigmosus in their early Carnian Assemblage “F”, while Mueller et al. (2016) designated their Aulisporites astigmosus pollen assemblage zone as Julian 2 (lower Carnian), integrated with organic-carbon isotope data linked to the geomagnetic polarity time scale. Paterson et al. (2017) recorded Aulisporites astigmosus from an early Carnian core drilled in the Snadd Formation of off-shore Kong Karls Land; this occurrence is constrained by Re–Os geochronology from an underlying core at the same site. While generally typical of the early Carnian, Aulisporites astigmosus may have sporadic occurrences in the Echinitosporites iliacoides and the Protodiploxypinus decus composite assemblage zones of Ladinian and late Anisian age respectively (Vigran et al. 2014).

95 The FO of consistent Aulisporites astigmosus is taken here as the base of the Carnian.

96 The LO of sporadic Cordaitina gunyalensis is based on multiple records from the Norwegian Arctic, including Vigran et al. (1998, 2014) from the Svalis Dome, Barents Sea, where it was recorded in three Ladinian cores. No independent faunal evidence exists from the three Ladinian cores, but the cored intervals overlie upper Anisian successions dated by ammonoids. Occurrences of Cordaitina gunyalensis in shallow cores penetrating the Snadd Formation in the Sentralbanken High and offshore Kong Karls Land areas of the Barents Sea indicate a LO within the lower part of the Aulisporites astigmosus Composite Assemblage Zone. Rhenium–osmium geochronology from the latter location (Xu et al. 2014), indicates that the LO of Cordaitina gunyalensis is no older than earliest Carnian. On Spitsbergen, the species so far has not been reported above the Anisian, and its absence within Carnian strata may be due to poor preservation.

97 The LO of Cordaitina gunyalensis is taken here as 10% up from the base of the Carnian.

98 The LO of Echinitosporites iliacoides is based on multiple records from the Norwegian Arctic. It was recorded at Bjørnøya in beds with the ammonoid Daxatina cf. canadensis (Mørk et al. 1990), which is of early Carnian age. This horizon would previously have been placed in the Ladinian, but the base of the Carnian has been designated a GSSP defined by the lowest occurrence of the cosmopolitan ammonoid Daxatina (base of Daxatina canadensis Subzone, lowest subzone of Trachyceras Zone) (Gradstein et al. 2012). Hochuli et al. (1989) used the LO of Echinitosporites iliacoides as a good downhole marker, and Vigran et al. (2014) recorded it from various locations in the Norwe-gian Arctic. Paterson and Mangerud (2017, 2019) and Paterson et al. (2017) recorded it from several places in the Barents Sea.

99 The LO of Echinitosporites iliacoides is here taken as 10% up from the base of the Carnian.

100 The LO of Semiretisporis hochulii is based on multiple records from the Norwegian Arctic. It was noted by Mueller et al. (2016) from the lower De Geerdalen Formation in Spitsbergen. Paterson et al. (2018) recorded common occurrences of the taxon (as Semiretisporis sp. A) (in their Assemblage SBH-1) from cores in the lower De Geerdalen Formation in the Sentralbanken area, having the LO of its common occurrence coeval with the LO of Echinitosporites iliacoides. Paterson and Mangerud (2017) also recorded that this LO is coeval with the top of Echinitosporites iliacoides in the lowermost Snadd Formation (in their assemblage SBS-VII); they correlated it with Assemblage G of Hochuli et al. (1989), which is now assigned to the early Carnian based on new ammonoid evidence (see Vigran et al. 2014 for discussion). The LO of common Semiretisporis hochulii marks the top of Semiretisporis hochulii Zone of Paterson and Mangerud (2019).

101 The LO of common to abundant Semiretisporis hochulii is taken here as 10% up from the base of the Carnian.

102 The FO of common Podosporites vigraniae is based on multiple records from the Norwegian Arctic. The age assignment of this event approximately corresponds to the LO of Echinitosporites iliacoides, which is recorded in beds containing the early Carnian ammonoid Daxatina cf. canadensis (Mørk et al. 1990). Paterson and Mangerud (2019) described the Podosporites vigraniae Zone, originally described as the “Podosporites cf. amicus Assemblage” (Paterson et al. 2016). They recorded this taxon from the Snadd Formation at core 7534/4-U-1, Sentralbanken High, Barents Sea.

103 The FO of common Podosporites vigraniae is taken here as 10% up from the base of the Carnian.

104 The FO of sporadic Ricciisporites tuberculatus is based on multiple records from the Norwegian Arctic. Vigran et al. (2014) reported its FO as somewhat above the base of their Aulisporites astigmosus Composite Assemblage Zone and included it as part of the definition of that zone. The age assignment of this event approximately corresponds to the LO of Echinitosporites iliacoides, which is recorded in beds containing the early Carnian ammonoid Daxatina cf. canadensis (Mørk et al. 1990). Paterson and Mangerud (2017) recorded Ricciisporites tuberculatus in exploration wells from the Barents Sea, but not extending down to the LO of Echinitosporites ilicoides; the same is the case from the Sentralbanken area (Paterson et al. 2017). However, rare specimens have been recorded from the Ladinian Kobbe and Snadd formations, assigned to the Echinitosporites iliacoides Composite Assemblage Zone, in the southern Barents Sea (Vigran et al. 2014).

105 The FO of sporadic Ricciisporites tuberculatus is taken here as 10% up from the base of the Carnian.

106 The FO of consistent Camarozonosporites rudis is based on multiple records from the Norwegian Arctic. Vigran et al. (2014) recorded it somewhat above the base of, and as part of the definition of, their Aulisporites astigmosus Composite Assemblage Zone. Paterson and Mangerud (2015) recorded it ranging throughout the De Geerdalen Formation on Hopen. From the Kong Karls Land area, Paterson et al. (2017) recorded it throughout an early Carnian core drilled in the Snadd Formation constrained by Re–Os geochronology from an underlying core at this site. The age assignment of the consistent FO of Camarozonosporites rudis corresponds approximately to the LO of Echinitosporites iliacoides, which is calibrated to beds with the early Carnian ammonoid Daxatina cf. canadensis (Mørk et al. 1990). However, sporadic occurrences of Camarozonosporites rudis have been recorded in Barents Sea wells from the Anisian Kobbe and Steinkobbe formations, corresponding with the Protodiploxypinus decus (Vigran et al. 2014, p. 138, 140) and Triadispora obscura (Paterson and Mangerud 2017) composite assemblage zones.

107 The FO of consistent Camarozonosporites rudis is taken here as 10% up from the base of the Carnian.

108 The FO of rare Uvaesporites argentaeformis is based on multiple records from the Norwegian Arctic. Vigran et al. (2014) listed the species as appearing somewhat above the base of, but part of the definition of, their Aulisporites astigmosus Composite Assemblage Zone, to which they assigned an early to middle Carnian age. Paterson and Mangerud (2015) recorded rare Uvaesporites argentaeformis through the De Geerdalen Formation at Hopen, but did not record the range base because the base of the formation there is below sea level. The age assignment approximately corresponds to, or is close to, the LO of Echinitosporites iliacoides, which has a LO in beds with the early Carnian ammonoid Daxatina cf. canadensis (Mørk et al. 1990).

109 The FO of rare Uvaesporites argentaeformis is taken here as 10% up from the base of the Carnian.

110 This recently described taxon was previously recorded as Kyrtomisporis sp. A by Paterson et al. (2017, pl. 2, figs. 12–15) throughout an early Carnian core from the Snadd Formation in the Kong Karls Land area; the age is constrained by Re–Os geochronology from an underlying core at the site. The age assignment of the FO of Kyrtomisporis moerki corresponds approximately to, or near the FO of, Echinitosporites iliacoides in this core. It was later recorded from a core in the middle part of the De Geerdalen Formation in the Sentralbanken area (Paterson et al. 2018). Its short range makes it a very good marker, and it is a diagnostic component of the Podosporites vigraniae Zone of Paterson and Mangerud (2019).

11 The FO of Kyrtomisporis moerki is taken here as 10% up from the base of the Carnian.

112 Kyrtomisporis moerki (Kyrtomisporis sp. A of Paterson et al. 2017, pl. 2, figs. 12–15) was recorded throughout an early Carnian core from the Snadd Formation in the Kong Karls Land area; the age is constrained by Re–Os geochronology from an underlying core at the site. Kyrtomisporis moerki has so far not been recorded above the early Carnian. It was also recorded from a core in the middle part of the De Geerdalen Formation in the Sentralbanken area (Paterson et al. 2018). Its short range makes it a very good marker species.

113 The LO of Kyrtomisporis moerki is taken here as the base of the Tuvalian (upper Carnian).

114 The FO of consistent Kyrtomisporis spp. (Kyrtomisporis laevigatus, Kyrtomisporis gracilis and Kyrtomisporis speciosus) is based on multiple records in the Norwegian Arctic. The FOs of these taxa were recorded by Bjærke and Manum (1977) and Paterson and Mangerud (2015) from upper De Geerdalen Formation (Hopen Member; Lord et al. 2014) at Hopen. On Spitsbergen, Mueller et al. (2016) recorded the FO of Kyrtomisporis spp. somewhat below the Leschikisporis aduncus acme. The base of Kyrtomisporis spp. in the Sverdrup Basin is still unknown, but their occurrence was reported by Suneby and Hills (1988) in younger Triassic successions. Older occurrences of Kyrtomisporis laevigatus might represent misidentifications of Concavisporites crassexinus, Dictyophyllidites mortonii or Iraqispora labrata.

115 The FO of consistent Kyrtomisporis spp. (Kyrtomisporis laevigatus, Kyrtomisporis gracilis and Kyrtomisporis speciosus) is taken here as the base of the Tuvalian (upper Carnian).

116 The LO of Dyupetalum vicentinense is based on multiple records from the Norwegian Arctic. Although rare, it is recorded in many localities; its youngest occurrence was regarded as intra-Ladinian by Hochuli et al. (1989). However, rare specimens were recorded in younger successions by Paterson et al. (2017), from shallow-core material in the Snadd Formation, offshore Kong Karls Land. Rhenium– osmium geochronology from other cores in the region (Xu et al. 2014) indicate an age no older than earliest Carnian. Similarly, early Carnian occurrences have been noted in exploration wells and shallow stratigraphic cores from the southern Barents Sea and Sentralbanken High, respectively (Paterson and Mangerud 2017, Paterson et al. 2018).

117 The LO of Dyupetalum vicentinense is taken here as the base of the Tuvalian (upper Carnian).

118 The FO of dominant Leschikisporis aduncus is based on multiple records from the Norwegian Arctic. Bjærke and Manum (1977) first recorded this acme from outcrop sections on Hopen, and later Paterson and Mangerud (2015) and Paterson et al. (2015) recorded it from the middle De Geerdalen Formation, also from Hopen, approximately dated as late Carnian. Hochuli et al. (1989) noted that Leschikisporis aduncus is common in their “middle” Carnian Assemblage D. In Spitsbergen, Nagy et al. (2011), Vigran et al. (2014) and Mueller et al. (2014, 2016) recorded this event from the upper parts of the De Geerdalen Formation. This event is also recognized in cores from Sentralbanken area of the Barents Sea (Paterson et al. 2018) and in exploration wells (e.g., Hochuli and Vigran 2010; Vigran et al. 2014; Paterson and Mangerud 2017, 2019). Note that Paterson et al. (2017) recorded abundant, but not dominant, Leschikisporis aduncus in an early Carnian core drilled in the Snadd Formation from offshore Kong Karls Land. These Snadd Formation assemblages were more diverse and different from those on Hopen, which were totally dominated by Leschikisporis aduncus. The former are probably of older, early Carnian age, as they are constrained by Re–Os geochronology from an underlying core.

119 The FO of dominant Leschikisporis aduncus is taken here as the base of the Tuvalian (upper Carnian).

120 The FO of abundant Protodiploxypinus is based on multiple records from the Norwegian Arctic. It was recorded by Paterson and Mangerud (2015) from the upper De Geerdalen Formation (Hopen Member) on Hopen. They named their Protodiploxypinus Assemblage from this acme and assigned it a late Carnian (Tuvalian) age (see discussion in Paterson and Mangerud 2015). This event is also recognized in cores from Sentralbanken area in the Barents Sea (Paterson et al. 2018), and from exploration wells in the upper Snadd Formation in the southern Barents Sea (Hochuli and Vigran 2010; Paterson and Mangerud 2017, 2019).

121 The FO of abundant Protodiploxypinus is taken here as the base of the Tuvalian (upper Carnian).

122 The LO of abundant to dominant Leschikisporis aduncus is based on multiple records from the Norwegian Arctic. Paterson and Mangerud (2015) recorded this event in the De Geerdalen Formation, where Leschikisporis aduncus is abundant up to the base of the Hopen Member. They defined their L eschikisporis aduncus Assemblage partly from this event and assigned it a late Carnian (middle Tuvalian) age (see Paterson and Mangerud 2015). Nagy et al. (2011) recorded this event from the upper part of the same formation in Spitsbergen. It is also recognized as an important event in Barents Sea exploration wells (e.g., Hochuli and Vigran 2010; Vigran et al. 2014; Paterson and Mangerud 2017). As discussed by Paterson et al. (2018), the apparent lack of Leschikisporis aduncus in the Sverdrup Basin may be because the Carnian samples analyzed from wells in the Schei Point Formation (Fisher and Bujak 1975) are younger than the Leschikisporis aduncus acme. In the Russian Barents Sea, this taxon remains dominant until the Norian (Mørk et al. 1993), suggesting that its range top in the Norwegian Barents Sea is facies controlled (see Paterson et al. 2016 and Paterson and Mangerud 2019). Note that the LO of abundant to dominant Leschikisporis aduncus is corresponding the the FO, indicating that this was a short-lived event.

123 The LO of dominant Leschikisporis aduncus is taken here to correspond to the base of the Tuvalian (upper Carnian).

124 The FO of rare Rhaetogonyaulax (including Rhaetogonyaulax arctica and Rhaetogonyaulax rhaetica) is based on multiple records from the Norwegian Arctic. This includes records from the middle parts of the De Geerdalen Formation dated as late Carnian (Paterson and Mangerud 2015, 2019 and Paterson et al. 2016). Rhaetogonyaulax has been recorded in the Sverdrup Basin (Fisher and Bujak 1975; Bujak and Fisher 1976; Felix and Burbridge 1978) and Alaska (Wiggins 1973).

125 The FO of rare Rhaetogonyaulax is taken here as the base of the Tuvalian (upper Carnian).

126 The LO of consistent Schizaeoisporites worsleyi is based on multiple records from the Norwegian Arctic. This species was first described from the Carnian on Hopen (Bjærke and Manum 1977). Paterson and Mangerud (2015) later recorded it ranging to the top of the De Geerdalen Formation, just below the overlying ammonoid-dated Norian succession. Vigran et al. (1998) recorded it from three Ladinian cores in the Svalis Dome, Barents Sea. Vigran et al. (2014) found rare occurrences of Schizaeoisporites worsleyi in their Limbosporites lundbladiae Composite Assemblage Zone, which may be reworked. Schizaeoisporites worsleyi is generally recorded in low numbers, but it is very distinct and thus a good marker.

127 The LO of consistent Schizaeoisporites worsleyi is taken here as the base of the Norian.

128 The LO of sporadic Aulisporites astigmosus is based on multiple records from the Norwegian Arctic. Paterson and Mangerud (2015) recorded this species from the De Geerdalen Formation, occurring up to the base of the Hopen Member on Hopen. Vigran et al. (2014) defined an early to middle Carnian Aulisporites astigmosus Composite Assemblage zone. However, Paterson et al. (2018) refined the palynological zonation and verified the palynological division between the lower and middle Carnian suggested by Hochuli et al. (1989), designating zones SBH I to SBH III.

129 The LO of sporadic Aulisporites astigmosus is taken here as the base of the Norian.

130 The LO of abundant Protodiploxypinus is based on multiple records from the Norwegian Arctic. It was first recorded as a reliable first downhole occurrence by Hochuli et al. (1989), and as a typical component of their late Carnian Assemblage C. Protodiploxypinus was also recorded by Paterson and Mangerud (2015) from the upper De Geerdalen Formation (Hopen Member) at Hopen. They named their Protodiploxypinus Assemblage from this acme and assigned it to the latest Carnian (see discussion in Paterson and Mangerud 2015). Paterson and Mangerud (2017) recorded abundant Protodiploxypinus from exploration wells in the upper Snadd Formation in the Barents Sea.

131 The LO of abundant Protodiploxypinus is taken here as the base of the Norian.

132 The LO of consistent Illinites chitonoides is based on multiple records from the Norwegian Arctic. It was reported from within the middle De Geerdalen Formation by Vigran et al. (2014). However, Paterson and Mangerud (2015) recorded it to the top of the De Geerdalen Formation (i.e. top Hopen Member) on Hopen, a horizon that they assigned a latest Carnian (Tuvalian) age. Paterson et al. (2018) recorded sporadic occurrences of Illinites chitonoides up into the early Norian Flatsalen Formation in cores from the Sentral-banken High, Barents Sea.

133 The LO of consistent Illinites chitonoides is taken here as the base of the Norian.

134 The FO of common Rhaetogonyaulax (including Rhaetogonyaulax arctica and Rhaetogonyaulax rhaetica) is based on multiple records from the Norwegian Arctic (Mangerud et al. 2018). Paterson and Mangerud (2015) and Paterson et al. (2016) recorded common Rhaetogonyaulax from the base of the Flatsalen Formation, where ammonoids of the ammonoid Mojsisovicsites kerri Zone of Norian age are recorded. Note that on Hopen, the Rhaetogonyaulax arctica peak is older than the Rhaetogonyaulax rhaetica peak. However, we consider that the difference reflects paleoenvironmental conditions rather than stratigraphic range. Rhaetogonyaulax arctica favours conditions closer to shore, and is thus more abundant than Rhaetogonyaulax rhaetica during the early stages of a transgression. Rhaetogonyaulax rhaetica probably favours outer shelf settings because it is most abundant in association with maximum flooding surfaces (Paterson et al. 2016). This interpretation is consistent with the overall lower abundance of Rhaetogonyaulax rhaetica in more proximal localities in the Barents Sea area, as in the Nordkapp Basin (Paterson et al. 2018) and Sentralbanken area (Paterson et al. 2017). One of us (JB; Appendix C) has also recorded the FO of common Rhaetogonyaulax rhaetica in Norian sidewall core sample 9188 ft (2801 m) in the Fireweed 1 well off northern Alaska; the age is based on the occurrence of age-diagnostic miospores in the same interval.

135 The FO of common Rhaetogonyaulax is taken here as the base of the Norian.

136 The FOs of dinocysts Hebecysta brevicornuta, Heibergella aculeata, Heibergella asymmetrica, Heibergella salebrosacea, Noricysta fimbriata, Noricysta pannucea, Noricysta varivallata, Sverdrupiella baccata, Sverdrupiella manicata, Sverdrupiella mutabilis, Sverdrupiella ornaticingulata, Sverdrupiella raiaformis, Sverdrupiella sabinensis, Sverdrupiella septentrionalis, Sverdrupiella spinosa, and Sverdrupiella usitata are based on their occurrences in the oldest Norian sample (sidewall core 9188 ft; 2801 m) in the Fireweed 1 exploration well, offshore northern Alaska. The sample is dated as Norian based on associated miospore events shown for the well in Appendix C herein. The dinocyst species were originally described by Bujak and Fisher (1976) in eight Sverdrup Basin well sections that were assigned a Norian age based on associated miospore assemblages by Fisher and Bujak (1975). They also characterize strata dated as Norian based on associated miospore events in exploration wells Klondike OCS-Y-1482 (Chukchi Sea) and Romulus C-67 (Sverdrup Basin), but the absence of sidewall- or conventional-core samples in these wells precludes confident age assignment of their oldest occurrences.

137 Species of Hebecysta, Heibergella, Noricysta and Sverdrupiella are restricted to the Noricysta pannucea – Heibergella asymmetrica (PA) Subzone of the Triancoraesporites ancorae – Camarozonsporites laevigatus (AL) Zone of Suneby and Hills (1988). The PA Subzone occurs in the lower part of the Romulus Member of the Heiberg Formation exposed at McKinley Bay, Blackwelder Anticline, Fosheim Anticline and Raanes Peninsula on Elsemere Island, in strata assigned a Norian age by Embry (1982) based on bivalves and ammonoids.

138 Paterson and Mangerud (2015) recorded rare Sverdupiella from the base of the Flatsalen Formation on Hopen, where taxa of the Norian ammonoid Mojsisovicsites kerri Zone are recorded. As with Rhaetogonyalaux, the stratigraphic range of Sverdrupiella in the circum-Arctic region likely varies according to paleoenvironment: the genus is apparently more common and diverse in the Sverdrup Basin as shown above (e.g., Bujak and Fisher 1976; Suneby and Hills 1988), which was likely in closer communication with the open ocean compared to the Barents Sea area (Sømme et. al. 2018).

139 The FO of Hebecysta, Heibergella, Noricysta, Sverdrupiella is taken here as the base of the Norian.

140 The FO of Classopollis torosus is based on multiple records from the Norwegian Arctic. It is recorded from the base of the Flatsalen Formation on Hopen, a horizon assigned an early Norian age based on ammonoids typical of the Mojsisovicsites kerri Zone (Paterson and Mangerud 2015). The taxon also gave its name to Paterson and Mangerud’s Classopollis torosus Assemblage. Classopollis torosus was previously recorded by Smith et al. (1975) and Bjærke and Manum (1977) from Hopen Island. Paterson et al. (2017) reported the FO of Classopollis torosus in their Norian SBH-V Assemblage from Sentralbanken in the Barents Sea. Paterson and Mangerud (2017) reported common Classopollis torosus in their Norian Assemblage SBS-II based on exploration wells in the southern Barents Sea. In the Russian Barents Shelf, a similar influx in Classopollis is recorded at the base of the Norian T3k-n Zone (Fefilova 1988; Pavlov et al. 1985; Mørk et al. 1993).

141 The FO of Classopollis torosus is taken here as the base of the Norian.

142 The FO of sporadic Limbosporites lundbladiae is based on records from multiple localities in the Arctic; although relatively rare in the Norian, it seems to be a robust marker. Fisher and Bujak (1975) reported Limbosporites lundbladiae co-occurring with dinoflagellate-cyst assemblages typical for the Norian successions in the Sverdrup Basin, but their work was based mainly on cuttings samples, so that taxon bases are unreliable. Working on out-crop sections in the Sverdrup Basin, Suneby and Hills (1988) recorded Limbosporites lundbladiae ranging from within their oldest Norian SC Subzone in the Heiberg Formation, but did not study older sections to verify the true FO. From the Barents Sea area, Hochuli et al. (1989) reported the FO of Limbosporites lundbladiae in their Assemblage B-2 and Vigran et al. (2014) used the FO of this species as the base of their Norian Limbosporites lundbladiae Composite Assemblage Zone. Paterson and Mangerud (2015) also used the FO of abundant Limbosporites lundbladiae to define the base of their Limbosporites lundbladiae – Quadraeculina anellaeformis Assemblage, corresponding to basal Flatsalen Formation on Hopen, which is assigned an early Norian age based on ammonoids; however, Limbosporites lundbladiae occurs spor-adically from the base of the Flatsalen Formation. Pater-son et al. (2017) recorded a few specimens of Limbosporites lundbladiae from the uppermost De Geerdalen Formation from shallow cores in the Sentralbanken area; this occurrence is close to the Carnian/Norian transition.

143 The FO of sporadic Limbosporites lundbladiae is taken here as the base of the Norian.

144 The FO of sporadic Quadraeculinaanellaeformis is reported from multiple localities in the Arctic. Suneby and Hills (1988) recorded Quadraeculina anellaeformis ranging from within their oldest Norian SC Subzone in the Heiberg Formation, Sverdrup Basin; however, the FO is unknown, and the species ranges up into the Jurassic. From the Barents Sea area, Hochuli et al. (1989) reported the FO of Quadraeculina anellaeformis in their Assemblage B-2, while Vigran et al. (2014) reported the species from the base of their Limbosporites lundbladiae Composite Assemblage Zone, which corresponds to the base of the Norian. Paterson and Mangerud (2015) recorded the FO of sporadic Quadraeculina anellaeformis from the basal Flatsalen Formation on Hopen, a horizon assigned an early Norian age based on ammonoids typical of the Mojsisovicsites kerri Zone (Paterson and Mangerud 2015). However, Quadraeculina anellaeformis occurred more consistently from the base of the overlying Svenskøya Formation, from which they defined their Limbosporites lundbladiae – Quadraeculina anellaeformis Assemblage. Older rare occurrences of Quadraeculina anellaeformis have been recorded from the De Geerdalen Formation (Mueller et al. 2016) and in strata dated as late Carnian in cores from the Sentralbanken High area of the Barents Sea (Paterson et al. 2018).

145 The FO of sporadic Quadraeculina anellaformis is taken here as the base of the Norian.

146 The FO of consistent (to abundant) Riccisporites tuberculatus is based on records from Suneby and Hills (1988). However, Felix (1975) first recognized Riccisporites tuberculatus as an important stratigraphic marker in the Heiberg Formation on Ellef Ringnes Island, Sverdrup Basin. He reported abundant Riccisporites tuberculatus in all samples from the Triassic part of the formation. Later, Suneby and Hills (1988) reported Riccisporites tuberculatus from the base of their studied section (AL Biozone), dated as early Norian. From farther south, in East Greenland, Pedersen and Lund (1980) and Mander et al. (2013) recorded abundant Riccisporites tuberculatus from the Kap Stewart Formation, a classic Rhaetian plant-macro-fossil locality, but most likely representing a mixed flora. Paterson et al. (2017) reported Riccisporites tuberculatus from the basal Flatsalen Formation equivalent, based on core material from the Sentralbanken area, Barents Sea. On nearby Hopen Island, the lower part of the Flatsalen Formation was dated as early Norian based on ammonoids. Although the age of this FO is somewhat uncertain, its consistent FO is inferred to be at the base of the Norian.

147 FO of consistent Riccisporites tuberculatus is here taken here as the base of the Norian.

148 The LO of Kraeuselisporites cooksoniae is based on records by Paterson and Mangerud (2015) from Hopen, where this taxon was recorded to the top of the Flatsalen Formation; its LO is coeval with that of the dinoflagellate cyst Rhaetogonyaulax, occurring slightly above early Norian ammonoids.

149 The LO of Kraeuselisporites cooksoniae is taken here as 50% up from the base of the Norian.

150 The LO of Porcellispora longdonensis is based on data from Paterson and Mangerud (2015) from Hopen Island, where this taxon ranges to the top of the Flatsalen Formation, its LO being coeval with the LO of Rhaetogonyaulax. The LO of Porcellispora longdonensis occurs somewhat above early Norian ammonoids, but still below typical Rhaetian palynological assemblages at this location. A few specimens are reported in younger sections in the Hammerfest Basin (Vigran et al. 2014) and in the Sverdup Basin (Suneby and Hills 1988).

151 The LO of Porcellispora longdonensis is taken here as 50% up from the base of the Norian.

152 The FO of consistent Limbosporites lundbladiae is based on multiple reports from the Arctic and seems to be a robust marker. From outcrop sections in the Sverdrup Basin, Suneby and Hills (1988) recorded common Limbosporites lundbladiae from outcrop sections above typical Norian dino flagellate cyst assemblages and ranging up from within their oldest Norian SC Subzone in the Heiberg Formation, but with the FO unknown. Felix (1975) and Fisher and Bujak (1975) also reported Limbosporites lundbladiae but did not provide quantitative data. Hochuli et al. (1989) reported the lowest occurrence of Limbosporites lundbladiae in their Assemblage B-2. Vigran et al. (2014) named their Norian palynological zone the Limbosporites lundbladiae Compos-ite Assemblage Zone and defined the base of the zone on the FO of the species, equating the event with the base of the Norian. Paterson and Mangerud (2015) recorded the consistent FO of Limbosporites lundbladiae from the base of the Svenskøya Formation at Hopen and defined the base of their Limbosporites lundbladiae – Quadraeculina anellaeformis Assemblage at this level. They assigned to the event a ?late Norian age based on palynological evidence in combination with the age assignment of the underlying assem-blages. Pedersen and Lund (1980) also recorded abundant Limbosporites lundbladiae from the Kap Stewart Formation of East Greenland. Since independent age control is very limited in this part of the succession, age determination is problematic.

153 The FO of consistent Limbosporites lundbladiae is taken here as 50% up from the base of the Norian.

154 The FO of consistent (to common) Quadraeculina anellaeformis has been reported from multiple localities in the Arctic. From outcrop sections, Suneby and Hills (1988) reported Quadraeculina anellaeformis as ranging from within their oldest Norian SC Subzone in the Heiberg Formation, albeit with an unknown FO as they did not include older successions. They recorded Quadraeculina anellaeformis ranging up into the Jurassic. Paterson and Mangerud (2015) defined the base of their Limbosporites lundbladiae – Quadraeculina anellaeformis Assemblage as corresponding to the basal Svenskøya Formation, with Quadraeculina anellaeformis be-ing common in the upper part of the formation. The species has also been recorded as common from the Knorringfjellet Formation in Spitsbergen (Mueller et al. 2016).

155 The FO of consistent Quadraeculina anellaeformis is taken here as 50% up from the base of the Norian.

156 The FO of common to abundant Riccisporites tuberculatus is based on Suneby and Hills (1988), but the species was first recognized as an important stratigraphic marker by Felix (1975) in materials from Ellef Ringnes Island, Sverdrup Basin. He reported this species as abundant in all samples from the Triassic part of the Heiberg Formation. Suneby and Hills (1988) reported its common occurrence from the Heiberg Formation at the base of their LT Biozone, which is of latest Norian to early Rhaetian age. In the Barents Sea region, the FO of common Ricciisporites tuberculatus occurs above early Norian ammonoids and below typical Rhaetian palynological assemblages.

157 The FO of common Riccisporites tuberculatus is taken here as 50% up from the base of the Norian.

158 Paterson and Mangerud (2015) reported Polycingulatisporites crenulatus from the upper part of the Svenskøya Formation on Hopen, and tentatively correlated it with Assemblage A of Hochuli et al. (1989). It is a rare, but very distinct taxon, and its FO is probably of stratigraphic significance. As it co-occurs with the typical Triassic palynomorph Aratrisporites in “typical Rhaetian” palynological assemblages distinct from those in older strata, a Rhaetian age is inferred.

159 The FO of Polycingulatisporites crenulatus is taken here as the base of the Rhaetian.

160 The LOs of dinocysts Hebecysta brevicornuta, Heibergella aculeata, Heibergella asymmetrica, Heibergella salebrosacea, Noricysta fimbriata, Noricysta pannucea, Noricysta varivallata, Sverdrupiella baccata, Sverdrupiella manicata, Sverdrupiella ornaticingulata, Sverdrupiella raiaformis, Sverdrupiella sabinensis, Sverdrupiella septentrionalis, Sverdrupiella spinosa, and Sverdrupiella usitata are based on their occurrence in the youngest samples dated as Norian in exploration wells Fireweed 1 (offshore northern Alaska), Klondike OCS-Y-1482 (Chukchi Sea) and Romulus C-67 (Sverdrup Basin). This date is interpreted from miospore events that occur in the well sections (Appendix C). The dinocyst species are restricted to the Noricysta pannucea – Heibergella asymmetrica (PA) Subzone of the Triancoraesporites ancorae – Camarozonsporites laevigatus (AL) Zone defined by Suneby and Hills (1988). The PA Subzone occurs in the lower part of the Romulus Member of the Heiberg Formation exposed at McKinley Bay, Blackwelder Anticline, Fosheim Anticline and Raanes Peninsula on Elsemere Island in strata assigned a Norian age by Embry (1982) based on bivalves and ammonoids.

161 The LOs of Hebecysta brevicornuta, Heibergella aculeata, Heibergella asymmetrica, Heibergella salebrosacea, Noricysta fimbriata, Noricysta pannucea, Noricysta varivallata, Sverdrupiella baccata, Sverdrupiella manicata, Sverdrupiella ornaticingulata, Sverdrupiella raiaformis, Sverdrupiella sabinensis, Sverdrupiella septentrionalis, Sverdrupiella spinosa, and Sverdrupiella usitata are taken here as the base of the Rhaetian.

162 The LO of Ricciisporites umbonatus was reported by Suneby and Hills (1988) to occur slightly below the LO of Limbosporites lundbladiae and to be coeval with the LO of common Limbosporites lundbladiae and Ricciisporites tuberculatus. Vigran et al. (2014) also reported this event as intra-Rhaetian. Precise age assignment is difficult, but a relative occurrence of this event can be proposed based on experience.

163 The LO of Ricciisporites umbonatus is taken here to be 30% up from the base Rhaetian.

164 Suneby and Hills (1988) reported the LO of common Limbosporites lundbladiae at the top of their Limbosporites lundbladiae – Ricciisporites tuberculatus Biozone and suggested its age is latest Norian or early Rhaetian. However, they indicated uncertainty regarding the age assignment. Vigran et al. (2014) reported the LO of common Limbosporites lundbladiae as an intra-Rhaetian event. Paterson and Mangerud (2015) defined their Limbosporites lundbladiae – Quadraeculina anellaeformis Assemblage from the Svenskøya Formation and recorded common Limbosporites lundbladiae to the top of the formation. Since there have been no reports of Limbosporites lundbladiae from the Jurassic, this LO is inferred to coincide with the base of the Jurassic.

165 The LO of common Limbosporites lundbladiae is taken here as the base of the Jurassic.

166 The LO of Aratrisporites has been reported from the Sverdrup Basin (Felix 1975, Suneby and Hills 1988), with its LO at the top of the Triassic (within the Heiberg Formation). Vigran et al. (2014) also listed several species of Aratrisporites as having their LO at the top of the Triassic. Paterson and Mangerud (2015) recorded several Aratrisporites species in their uppermost samples from the Svenskøya Formation on Hopen, including Aratrisporites scabratus, Aratrisporites laevigatus, Aratrisporites macrocavatus and Aratrisporites tenuispinosus. To our knowledge, there are no records of Aratrisporites younger than Triassic in the circum- Arctic region.

167 The LO of Aratrisporites is taken here at the base of the Hettangian (Jurassic).

168 The LO of taeniate bisaccate pollen has been reported from multiple localities from the Arctic. Vigran et al. (2014) used the LO of taeniate bisaccate pollen as a top Triassic event. Suneby and Hills (1988) listed Lunatisporites rhaeticus (as Taeniasporites rhaeticus) as extending to the top of the Triassic in the Sverdrup Basin. That species was also recorded by Felix (1975) and Paterson and Mangerud (2015), the latter authors recording it as a single specimen in their uppermost sample from the Norian–Rhaetian Svenskøya Formation on Hopen.

169 The LO of taeniate bisaccate pollen is taken here at the base of the Hettangian (Jurassic).

170 Sverdrupiella mutabilis has a longer stratigraphic range than other species of Sverdrupiella. Its LO is based on their occurrence in the youngest samples dated as Norian in the wells Fireweed 1 (offshore northern Alaska), Klondike OCS-Y-1482 (Chukchi Sea) and Romulus C-67 (Sverdrup Basin) in which its age assignment is constrained by Triassic miospore and Jurassic events that occur in the underying and overlying sections (Bujak et al., in press c).

171 The LO of Sverdrupiella mutabilis is taken here at the base of the Hettangian (Jurassic).