The identification of one specimen of Retispora lepidophyta within strata of the Plantekløfta Formation by Brinkmann (1997, Table 14.3 therein) and Piepjohn et al. (2000; published in Schweitzer, 1999, Plate 6 in their Fig. 10 and Plate 7 in their Fig. 1) suggests a late Famennian age for the top of the Plantekløfta Formation and hence that Svalbardian tectonism terminated during the Famennian to Tournaisian in northern and central Spitsbergen.

Recent studies clearly demonstrated that the interpretation of Retispora lepidophyta by Brinkmann (1997), Schweitzer (1999), and Piepjohn et al. (2000) is erroneous. Notably, the lone figured specimen interpreted as Retispora lepidophyta by Schweitzer (1999) and Piepjohn et al. (2000) differs in size and shows significantly different morphological structures from typical Retispora lepidophyta (Playford, 1976; Berry and Marshall, 2015, Supplement DR3 therein; see also Supplement S1). In addition the fovea that characterize the spore's exoexine appear to be the result of damage by cubic diagenetic pyrite. Attempts have been made to locate the Retispora lepidophyta specimen figured in Brinkmann (1997) and Schweitzer (1999) and used by Piepjohn et al. (2000) to date Svalbardian tectonism in central Spitsbergen for further analysis. These attempts were unfortunately unsuccessful (Marshall, J. E. A., personal observation, 2020).

Berry and Marshall (2015) re-evaluated the age of the Plantekløfta Formation to be early Frasnian based on fossils and miospores (ca. 383–380 Ma; see also their Supplements; Fig. 2). In addition, the paleontological study of Newman et al. (2019, 2020, 2021) recorded the presence of articulated fish in the Fiskekløfta Member of the Tordalen Formation (Fig. 2), i.e., undoubtedly in situ fossils, demonstrating a late to latest Givetian (ca. 385–383 Ma; Middle Devonian) age for this stratigraphic unit instead of late Famennian. If the relatively coarse grain size of the sedimentary deposits of the Planteryggen and Plantekløfta formations indeed reflects the onset of Svalbardian tectonism as suggested by Piepjohn and Dallmann (2014), the new paleontological and palynological ages constrain the initial phase of the Svalbardian Orogeny at 383–380 Ma.

A late Famennian age for the Plantekløfta Formation based on the lone specimen of Retispora lepidophyta in central Spitsbergen is the only contradictory evidence against a mid-Famennian age for the base of the Billefjorden Group and older age for the Mimerdalen Subgroup (Scheibner et al., 2012; Lindeman et al., 2013; Berry and Marshall, 2015; Marshall et al., 2015; Lopes et al., 2019; Newman et al., 2019; Lopes, G., personal observation, 2019).

Recent palynological studies in central Spitsbergen dated the base of the Billefjorden Group in Triungen (see Fig. 1 for location) to the mid-Famennian (maximum ca. 365 Ma; Lindemann et al., 2013; Marshall et al., 2015; Lopes, G., personal observation, 2019; Fig. 2). At least 30 samples contained characteristic Famennian spore assemblages including Cyrtospora cristifer, Cornispora monocornata, Cornispora bicornata, Cornispora tricornata, Lophozonotriletes lebedianensis, Knoxisporites dedaleus, Grandispora gracilis, Spelaeotriletes papulosus, Cristatisporites lupinovitchi, Lagenosisporites sp., Grandispora famensis, and Tergobulasporites immensus (Marshall et al., 2015). Some samples from the lower part of the Billefjorden Group in Billefjorden also contained Retispora lepidophyta (Lopes, G., personal observation, 2019). These spore assemblages were also identified in sedimentary rocks in the lower part of the Billefjorden Group in northeastern Spitsbergen (Scheibner et al, 2012), thus strengthening a Famennian age for the base of this stratigraphic unit throughout northern and central Spitsbergen. Note that the base of the Billefjorden Group in Bjørnøya was also dated as Famennian based on palynology (Kaiser, 1970; Worsley and Edwards, 1976; Lopes et al., 2021). This strongly suggests that the Svalbardian deformation, which ended prior to the deposition of the Billefjorden Group (Piepjohn, 2000), must have been terminated by the mid-Famennian in central and northern Spitsbergen. This implies a maximum duration of 18 Ma for this tectonic event.

Piepjohn and Dallmann (2014) proposed that the mid- to late-Famennian spores identified in the lower part of the Billefjorden Group were reworked based on their identification of one specimen of Retispora lepidophyta within the Plantekløfta Formation (Piepjohn et al., 2000). However, since this specimen clearly is a misidentification (Berry and Marshall, 2015, Supplement DR3 therein), the claim of reworking of mid- to late-Famennian spores found within the base of the Billefjorden Group in Triungen no longer has any supporting argument in Svalbard, and neither does the claim of Piepjohn et al. (2000) that the older Devonian spores found in the sample with the misidentified specimen of Retispora lepidophyta were reworked.

At least some of the deformation in Lower to lowermost Upper Devonian strata of the Andrée Land Group and Mimerdalen Subgroup in central and northern Spitsbergen is early Cenozoic in age because uppermost Devonian to Mississippian strata of the Billefjorden Group, which overlie the Andrée Land Group and Mimerdalen Subgroup in the area, are intensely sheared top-west, e.g., in Pyramiden (Koehl, 2021) and Garmdalen (Koehl et al., 2020, 2022b; locations in Fig. 1). This is further supported by the interpretation of seismic data adjacent to nearshore portions of Billefjorden showing the presence of a bedding-parallel décollement between the Wood Bay Formation and the Gipsdalen Group (Koehl et al., 2020). These suggest a significant impact of strain partitioning during Eurekan deformation. Eurekan strain partitioning is further illustrated by tight plastic folding of Lower Devonian strata of the Andrée Land Group and brittle brecciation of the unconformity with Upper Pennsylvanian to Permian strata in Yggdrasilkampen (Manby et al., 1994, Fig. 11 therein) and by décollements within Middle Devonian deposits near the Billefjorden Fault Zone in Wijdefjorden (Marshall, J. E. A., personal observation, 2022; see Fig. 1 for location).

Another argument corroborating these data is the involvement in folding of Carboniferous picritic dikes dated at ca. 357 Ma (Evdokimov et al., 2006; monchiquite dikes in Gayer et al., 1966, and Manby and Lyberis, 1996) intruding Lower Devonian sedimentary rocks at Krosspynten (see location in Fig. 1).

In addition, part of the deformation recorded by Lower to lowermost Upper Devonian strata of the Andrée Land Group and Mimerdalen Subgroup is possibly related to extensional detachment folding in the Devonian (Chorowicz, 1992; Roy, 2007, 2009; Roy et al., 2022). This is also supported by recent field and geochronological studies in northwestern Spitsbergen (Braathen et al., 2018, 2020; Maher et al., 2022).

Thus, it is unclear how much (if any at all) of the deformation observed within Lower to lowermost Upper Devonian strata of the Andrée Land Group and Mimerdalen Subgroup in central and northern Spitsbergen actually reflects Ellesmerian tectonism.

In southern Spitsbergen, Lower to Middle Devonian sedimentary rocks of the Marietoppen Formation (time equivalent to the Pragian to Eifelian Wood Bay and Grey Hoek formations of the Andrée Land Group in central and northern Spitsbergen; Fig. 2) unconformably overlie Precambrian to early Paleozoic basement rocks and are overlain by sedimentary strata of the Adriabukta Formation that were deformed into tight east-verging folds presumably during Svalbardian tectonism (Birkenmajer, 1964). The age of the Adriabukta Formation was dated to the Middle Mississippian through analysis of palynomorphs from black shales at the base and within the formation (Birkenmajer and Turnau, 1962; Fig. 2). Dallmann et al. (1999) noted that because of the age discrepancy between the Middle Mississippian Adriabukta Formation and the Lower to lowermost Upper Devonian Andrée Land Group in central and northern Spitsbergen, the folding of the Adriabukta Formation could not be correlated to Svalbardian folding. Nevertheless, in 2011, Dallmann suggested that the Adriabukta Formation is actually Late Devonian in age based on structural correlation between presumed Svalbardian structures in the Adriabukta Formation and Svalbardian fold-and-thrust belts in central and northern Spitsbergen, thus generating a debate around the actual age of the formation. This is referenced as “Dallmann, W., personal communication (2009)” in Bergh et al. (2011).

The speculation and debate initiated by Dallmann around the age of the Adriabukta Formation is based on neither published material nor specific scientific evidence. By contrast, Birkenmajer and Turnau (1962) identified a count of 350 spore specimens from the Adriabukta Formation including specimens of Lycospora, Tripartites, and Triquitrites, which were then and are still characteristic of the Middle Mississippian (Hughes and Playford, 1961; Playford, 1962, 1963; Clayton 1996). Later palynological studies in Svalbard (Billefjorden; Lopes et al., 2019) and Europe (Clayton et al., 1977) corroborate the Middle Mississippian ages obtained by Birkenmajer and Turnau (1962) for the Adriabukta Formation. Thus, the debate around the Middle Mississippian ages obtained for the Adriabukta Formation by Birkenmajer and Turnau (1962) is not justified, and a Middle Mississippian age is entirely justified. The Adriabukta Formation in southern Spitsbergen is therefore a time-equivalent example for the Billefjorden Group (e.g., Lopes et al., 2019).

The Middle Mississippian age of the Adriabukta Formation suggests that folding within this stratigraphic unit cannot be Late Devonian and is therefore not related to Svalbardian tectonism. A more likely origin for deformation within the Adriabukta Formation is the early Cenozoic Eurekan tectonic event. The tightly folded character of the Adriabukta Formation was previously proposed to be related to the dominance of weak shale and to Cenozoic strain partitioning by Birkenmajer and Turnau (1962). This scenario is now the most likely explanation for differential deformation of shales of the Adriabukta Formation and for folding of the Marietoppen Formation in southern Spitsbergen.

In Hornsundneset (Fig. 1), Siedlecki and Turnau (1964) analyzed eight samples from the Hornsundneset and Sergeijevfjellet formations of the Billefjorden Group. They proposed a Serpukhovian (Late Mississippian) age based on palynological results. However, a re-evaluation of their results showed that the Billefjorden Group in Hornsundneset (location in Fig. 1) is Middle Mississippian in age (Dallmann et al., 1999; Krajewski and Stempien-Salek, 2003), i.e., contemporaneous with the Adriabukta Formation (Fig. 2).

Interestingly, the Hornsundneset and Sergeijevfjellet formations are dominated by relatively hard, flat-lying beds of sandstone. Though located closer to the early Cenozoic collision zone with Greenland (i.e., within the West Spitsbergen Fold-and-Thrust Belt), these formations are relatively undeformed compared to the shale-dominated Adriabukta Formation (Siedlecki, 1960). This further supports a significant impact of strain partitioning on deformation patterns during the Eurekan tectonic event in southern Spitsbergen.

In Adriabukta (location in Fig. 1), the Adriabukta Formation is truncated by a major shear zone, the Mariekammen Shear Zone, which comprises hundreds of meter-long lenses of Cambrian metasedimentary basement rocks, shows a top-east reverse sense of shear and is unconformably overlain upwards by mildly folded Pennsylvanian strata of the Gipsdalen Group (Hyrnefjellet Formation), thus possibly reflecting Svalbardian tectonism (Birkenmajer and Turnau, 1962; Birkenmajer, 1964; Dallmann, 1992; Bergh et al., 2011). However, these previous studies did not account for the impact of Eurekan tectonism in southern Spitsbergen. A simple restoration of the shear zone prior to Eurekan deformation shows that, if this structure is indeed Mississippian in age, it must have formed as a normal fault and therefore cannot reflect Svalbardian contractional deformation (Supplement S2). It should be noted that other workers proposed that the Mariekammen Shear Zone formed as an early Cenozoic structure (Dallmann, 1992; von Gosen and Piepjohn, 2001). The fact that the shear zone does not seem to crosscut the Hyrnefjellet Formation and instead abruptly dies out at the unconformity (see sketch in Fig. 5 in Bergh et al., 2011) instead supports a formation as a normal fault in the Mississippian (Supplement S2).

The Adriabukta Formation was intruded by two, thin, bedding-parallel, Early Cretaceous dolerite sills of the Diabasodden Suite (Senger et al., 2013) that are folded together with bedding surfaces (Birkenmajer and Morawski, 1960; Birkenmajer, 1964). If the Adriabukta Formation was already folded in the Early Cretaceous, the sills would have truncated both fold structures and bedding surfaces. For sills to intrude along bedding surfaces, these must have remained relatively undeformed, sub-planar, and sub-horizontal until the Early Cretaceous. The Early Cretaceous sills and Middle Mississippian sedimentary strata were then folded together during subsequent Eurekan deformation. The two Early Cretaceous sills therefore further constrain the age of folding within the Adriabukta Formation and Marietoppen Formation to the early Cenozoic.

An early Cenozoic age for folding of shales of the Adriabukta Formation is further suggested by similar tight, east-verging fold geometries in Lower Triassic sedimentary strata incorporated as lenses into basement rocks in Fiskeknatten (location shown in Fig. 1; Birkenmajer, 1964).

Svalbardian deformation may be recorded in southernmost Spitsbergen (Røkensåta; Fig. 1 for location) where two outcrops of limited geographical extent (<1 km2) show poorly exposed, gently dipping, shale-rich, Lower Triassic sedimentary rocks over folded Middle Devonian strata (Dallmann, 1992). However, the two outcrops are of small size because they were extensively eroded, and the stratigraphic contact between Devonian and Triassic rocks is completely covered by loose material and located on steep mountain flanks (i.e., inaccessible for detailed inspection). In addition, Triassic successions in Spitsbergen dominantly consist of weak shale (Worsley and Mørk, 1978), which localized large amounts of Eurekan deformation and displacement along décollement levels, and strain partitioning during early Cenozoic contraction is now known to have had a considerable influence on the deformation of shale units in southern Spitsbergen (e.g., tightly folded Middle Mississippian Adriabukta Formation versus undeformed Middle Mississippian Hornsundneset Formation; Siedlecki, 1960; Birkenmajer and Turnau, 1962). Furthermore, folds within Middle Devonian rocks in Røkensåta appear to die out upwards (see Fig. 4a in Dallmann, 1992). It is therefore possible that deformation in Røkensåta is also early Cenozoic in age.

Such heavily eroded and limited outcrops need to be interpreted with extreme caution. Lower Triassic strata throughout Spitsbergen are well known for hosting bedding-parallel Eurekan décollements (Maher, 1984; Maher et al., 1986, 1989; Andresen et al., 1988; Bergh and Andresen, 1990; Haremo et al., 1990; Haremo and Andresen, 1992; Andresen et al., 1992; Dallmann et al., 1993; Bergh et al., 1997). The most spectacular examples include the décollement in dark shales on the Midterhuken Peninsula (Maher, 1984; Dallmann et al., 1993; location shown in Fig. 1), the Berzeliustinden thrust in southern Spitsbergen (Dallmann, 1988), the Triassic décollement penetrated by the 7816/12-1 exploration well and well imaged on seismic data in Reindalspasset (Eide et al., 1991; Koehl, 2021, Fig. 5g therein; see Fig. 1 for location), and the “Lower Décollement Zone” in eastern Spitsbergen (Haremo et al., 1990; Andresen et al., 1992; Haremo and Andresen, 1992). A similar structure may very well have decoupled Eurekan deformation between folded Middle Devonian and overlying gently dipping Lower Triassic sedimentary strata in Røkensåta. Triassic shales are known to be much weaker than Devonian shales and to have preferentially localized Eurekan deformation at a much lower scale (e.g., décollements with kilometer-scale displacement in the Triassic shales versus open meso- to macro-scale folds with limited to no displacement within Devonian shales). This example stresses the importance of detailed inspection of extensively eroded outcrops, especially in glaciated Arctic areas, and highlights potential flaws in long-distance interpretation of kilometer-scale mountain flanks. Therefore, we propose that little to no weight should be given to any interpretation of these two poorly exposed and inaccessible outcrops until further inspection of the contact is made from very close range (e.g., using a drone).

In western Spitsbergen, Thiedig and Manby (1992) and Kempe et al. (1997) showed that west-verging thrusts crosscut Proterozoic and Devonian sedimentary rocks in Blomstrandhalvøya (location in Fig. 1). They used the westwards transport direction of these thrusts to suggest that they record Svalbardian tectonism because it is comparable to observations along inferred Svalbardian thrusts in Dickson Land and Andrée Land in central and northern Spitsbergen (Vogt, 1938; Harland et al., 1974; Piepjohn, 2000).

In addition, Kempe et al. (1997) also noted the presence of small NW-verging thrusts on Blomstrandhalvøya. Notably, they argued that the size of these thrust was different from that of Svalbardian structures and concluded that they must therefore be post-Devonian. Kempe et al. (1997) argued that, even though the NW-verging thrusts seemed to have formed in the early Cenozoic, NW-directed transport directions are not typical of early Cenozoic Eurekan tectonism, which produced NE-verging thrusts and folds in adjacent areas of Brøggerhalvøya (Bergh et al., 2000; Piepjohn et al., 2001; see location in Fig. 1). They therefore proposed that NW-verging thrusts on Blomstrandhalvøya formed during a discrete tectonic event in the Pennsylvanian to Cretaceous. However, such a tectonic event is, thus far, unheard of in Spitsbergen. It is therefore more likely that the NW-verging thrusts in Blomstrandhalvøya formed in the early Cenozoic.

Previous works (e.g., Kempe et al., 1997) used the strike and vergence of structures in Blomstrandhalvøya to distinguish Eurekan from presumed Svalbardian structures. This argument is not valid because a single tectonic event may very well produce structures with varying vergence and strikes, e.g., the Eurekan in Svalbard, which resulted in the formation of east-verging structures in western and southwestern Spitsbergen (e.g., Maher et al., 1986; Dallmann et al., 1988, 1993; Andresen et al., 1994) and northeast-verging folds and thrusts in Brøggerhalvøya (e.g., Bergh et al., 2000; Piepjohn et al., 2001). Furthermore, recent regional studies have shown the occurrence of major, WNW–ESE-striking, several to tens of kilometers thick, thousands of kilometers long, inherited Timanian thrust systems extending from northwestern Russia to western Svalbard (Koehl, 2020; Koehl et al., 2021; Koehl et al., 2022a). One of these structures, the NNE-dipping Kongsfjorden–Cowanodden fault zone, extends into Kongsfjorden, where it was reactivated during the Caledonian and Eurekan events as a sinistral-reverse oblique-slip fault, thus partitioning deformation between northern and southern to western Svalbard during those two events and leading to oppositely verging Eurekan thrust across (e.g., west-verging in Andrée Land and Blomstrandhalvøya and east-verging in Røkensåta and Adriabukta and Hornsund) the fault and to bending Eurekan structures in the vicinity of the fault (e.g., in Brøggerhalvøya).

In western Blomstrandhalvøya, one sample in a presumably undeformed karst infill within a fissure in Proterozoic basement marbles that is a few meters wide yielded a Pennsylvanian to Permian age based on conodont fauna (Buggisch et al., 1994; Fig. 2). Since the karst infill was apparently not deformed, Buggisch et al. (1994) argued that the conodont fauna potentially constrained the formation of folds and west-verging thrusts on Blomstrandhalvøya to the Late Devonian (Svalbardian).

Nevertheless, several aspects of this feature call for caution regarding its bearing for Svalbardian tectonism. First, despite being located in an area deformed by Eurekan tectonism, e.g., Blomstrandhalvøya (e.g., NW-verging thrusts of Kempe et al., 1997) and Brøggerhalvøya; (Bergh et al., 2000; Piepjohn et al., 2001; Fig. 1), the Pennsylvanian to Permian cave seems to have escaped early Cenozoic deformation. This is possibly due to partitioning of Eurekan strain, which is known to have had a significant influence on deformation patterns in Brøggerhalvøya (e.g., Bergh et al., 2000). Thus, this small-scale karst feature is not an appropriate marker to discuss the timing of regional tectonic events in Blomstrandhalvøya.

Second, the cave is located within relatively undeformed Proterozoic marbles and away from presumed Svalbardian west-verging thrusts and associated deformed Lower Devonian sedimentary rocks on Blomstrandhalvøya. Hence, the karst infill is inappropriate to constrain the timing of Svalbardian deformation in Blomstrandhalvøya. The deformation in basement marble (if there is any at all at the location of the karst) could very well be Caledonian as previously suggested by Michalski (2018).

Third, the karst is the only one of its kind yielding a Pennsylvanian to Permian age and is, moreover, based on only one sample with a poorly preserved conodont fauna (Buggisch et al., 1994). In their study, Buggisch et al. (1994) specified that the assignation to published species was difficult due to the poor preservation of the elements. Hence, further studies of caves and conodont fauna on Blomstrandhalvøya are therefore needed to further assess the reliability of the age obtained by Buggisch et al. (1994) and its implication (if any at all) for Svalbardian tectonism. Considering all pieces of evidence gathered thus far, the folds and thrusts in Proterozoic to Lower Devonian rocks in Blomstrandhalvøya may all be Caledonian and Eurekan in age since no appropriate constraints are available to date any potential Svalbardian deformation.

In Prins Karls Forland (see Fig. 1 for location), amphibolite facies metamorphism was dated to 373–355 Ma by ion microprobe and 40Ar–39Ar geochronology and was postulated to be prograde and thus to record deep-crustal Svalbardian tectonism (ca. 15 km depth; Majka and Kośmińska, 2017; Faehnrich et al., 2017; Schneider et al., 2018; Kośmińska et al., 2020). This episode of deep-crustal metamorphism is coeval with shallow-crustal Svalbardian tectonism in central and northern Spitsbergen dated to ca. 383–365 Ma by recent paleontological and palynological studies (Scheibner et al., 2012; Lindemann et al., 2013; Marshall et al., 2015; Berry and Marshall, 2015; Newman et al., 2019; Lopes, G., personal observation, 2019). However, none of the ages in Prins Karls Forland are of any use in discussing the timing of the Svalbardian event since they could either reflect crustal thickening or late- to post-orogenic collapse.

Kinematic indicators along the dated west-dipping shear zone display top-SW to top-NW normal sense of shear (Schneider et al., 2018, Fig. 3b, e and f therein), which is incompatible with a formation during contractional (Svalbardianrian) tectonism. Instead, the shear sense suggests a close relationship with Devonian extensional collapse of the Caledonides. Notably, amphibolite facies metamorphism in Prins Karls Forland is also coeval with and occurred at comparable depth as deep-crustal, late Caledonian, high-pressure metamorphism along the conjugate eastern to northeastern Greenland margin (Gilotti et al., 2004; McClelland et al., 2006; Augland et al., 2010, 2011), which developed synchronously with the deposition of Devonian to Mississippian collapse basins along low-angle extensional detachments at the surface (Stemmerik et al., 1991, 1998, 2000; Larsen and Bengaard, 1991; Strachan, 1994; Larsen et al., 2008). During late- to post-orogenic collapse, deep contractional tectonics occurring typically at greenschist to amphibolite facies conditions (Snoke, 1980; Lister and Davis, 1989; Krabbendam and Dewey, 1998) are commonly associated with near-surface extension (Platt, 1986; Rey et al., 2001, 2011; Teyssier et al., 2005).

Amphibolite facies metamorphism in Prins Karls Forland was also coeval with collapse-related core complex exhumation in northwestern Spitsbergen (latest movement at 368 Ma; Braathen et al., 2018). Hence, despite the postulated prograde character of amphibolite facies metamorphism in Prins Karls Forland, its timing appears to coincide with Late Devonian extensional events in nearby areas. If the postulated prograde character of amphibolite facies metamorphism in Prins Karls Forland is to be reconciled with the observed overall top-SW to top-NW normal sense of shear (Schneider et al., 2018, Fig. 3b, e and f therein) and with extensional tectonics in northwestern Spitsbergen (Braathen et al., 2018), then the shear zone and associated prograde metamorphism may reflect gradual burial linked to the deposition of thick collapse sediments and/or normal movements along the shear zone.

Since the Late Devonian to Mississippian (373–355 Ma) amphibolite facies metamorphism in basement rocks in Prins Karls Forland probably occurred at ca. 15 km depth, the timing and nature of metamorphism may not have any implications for the nature of paleostress and resulting deformation in shallow-crustal Devonian sedimentary rocks in Spitsbergen (e.g., coeval ultra-high-pressure metamorphism at depth and extensional collapse at the surface in Greenland in the Devonian to Mississippian; Strachan, 1994; Gilotti et al., 2004; McClelland et al., 2006).

Furthermore, the geochronological ages obtained by Kośmińska et al. (2020) show broad ranges (430–336 Ma for monazite population I, 419–261 Ma for population II, and 443–226 Ma for population III) all ranging from the Silurian (Caledonian?) to the Carboniferous–Triassic. In addition, the ages obtained are associated with large σ1 errors (12.4–20.2 Myr for population I, 19.6–49.9 Myr for population II, and 17.1–64.4 Myr for population III; see online supplement S1 in Kośmińska et al., 2020). Since the length of Svalbardian tectonism in shallow-crustal Lower to lowermost Upper Devonian sedimentary rock in central and northern Spitsbergen is constrained to a maximum time span of 18 million years (383–365 Ma), i.e., a time span comparable with the σ1 errors associated with the ages obtained by Kośmińska et al. (2020), these ages are inappropriate to discuss the timing of Svalbardian tectonism in Svalbard (Schaltegger et al., 2015).

Geochronological ages in Oscar II Land (location in Fig. 1) are also useless in discussing the timing of the Svalbardian event since they may equally reflect extensional processes. Greenschist facies metamorphism that yielded 365–344 Ma 40Ar–39Ar and U–Th–Pb ages (Barnes et al., 2020) were re-evaluated to ca. 410 Ma (Early Devonian) by Ziemniak et al. (2020), who obtained comparable ages for the same unit without the 365–344 Ma disturbance, which they attribute to fluid circulation. This is also partly supported by the poorer statistical reliability of the 365–344 Ma ages as documented by Barnes et al. (2020). The 365–344 Ma episode of low-grade metamorphism was coeval with the deposition of Lower Devonian sedimentary rocks in central and northern Spitsbergen in the Devonian Graben during late–post-orogenic collapse of the Caledonides and thus may also be related to extensional processes (Gee and Moody-Stuart, 1966; Friend et al., 1966; Friend and Moody-Stuart, 1972; Murascov and Mokin, 1979; Manby and Lyberis, 1992; Friend et al., 1997; McCann, 2000).

In addition, Michalski et al. (2017) provided evidence of two episodes of thermal overprints at 377–326 and ca. 300 Ma in pre-Caledonian rocks in Oscar II Land using 40Ar–39Ar geochronology. The latter event is believed to be related to rifting. The former event at 377–326 Ma partly overlaps with the presumed timing of the Svalbardian Orogeny in central and northern Spitsbergen at ca. 383–365 Ma (Scheibner et al., 2012; Lindemann et al., 2013; Marshall et al., 2015; Berry and Marshall, 2015; Newman et al., 2019; Lopes, G., personal observation, 2019) and with the timing of 373–355 Ma amphibolite facies metamorphism in western Spitsbergen (Majka and Kośmińska, 2017; Faehnrich et al., 2017; Schneider et al., 2018; Kośmińska et al., 2020). It is, however, not possible to infer tectonic stress orientation, and this event may very well be related to Svalbardian tectonism or to late Caledonian extensional processes in northeastern Greenland and Prins Karls Forland (Stemmerik et al., 1991, 1998, 2000; Larsen and Bengaard, 1991; Strachan, 1994; Larsen et al., 2008; Schneider et al., 2018; see also previous section) and in northern Spitsbergen (Chorowicz, 1992; Roy, 2007, 2009; Braathen et al., 2018, 2020; Roy et al., 2022; Maher et al., 2022).