Polarforschung 68: 141 - 151,1998 (erschienen 2000)
The Ellesmerian and Caledonian Orogenie Belts of Greenland
By A.K. Higgins', NJ. Soper? and A.G. Leslie'
THEME 7: Problems of the CaledonianJEllesmerian Junction EAST GREENLAND CALEDONIDES
Summary: The 1300 km long N-S trending East Greenland Caledonides Survey mapping of the East Greenland Caledonides has dem comprises a western thin-skinned fold and thrust belt eharacterised by a pile 01' onstrated a straightforward essentially conventional architecture. flat lying thrust sheets displaced to the west 01' north-west, and an eastcrn thick skinned zone dominared by erystalline basement rocks. Erosion ofthe emersent The western marginal zone of the fold belt throughout its length . e Calcdonian thrust sheets commenced in mid-Llandovery time and produeed the comprises a marginal thin-skinned fold and thrust belt in which thick Silurian flysch deposits whieh filled the deep marine trouzh 01' the autochthonous 01' parautochthonous windows are intermittently Franklinian Basin which extended westwards across North Greenland into the exposed along the margin of the Inland lee (Fig. 2); these Canadian Aretic Islands. Deposition in the Franklinian Basin was brought to a close in the latest Devonian by the Ellesmerian orogeny, which produced the windows are distinguished by the presence of a thin, low grade, 600 kmlong E-W trending North Greenland fold belt. The sediments ofthe deep Proterozoic-Palaeozoic succession comparable to that in the water trough were displaeed southwards against the former platform margin foreland, and are overlain by a pile of high er grade thrust sheets. producing a southern thin-skinned fold and thrust belt. Deformation and The broad eastern segment of the Caledonian fold belt appears metamorphism increase in intensity northwards, and on the northern seaboard 01' Greenland there is a north-vergent Pa!eogene (Eurekan) overprint. to be essentially a thick-skinned thrust belt, dominated by deep Extensional faults which eontrolled development 01' the Franklinian Basin were seated crystalline basement rocks of Palaeoproterozoic origin reactivatecl by thrusting during the Ellesmerian orogeny, but in contrast to the reworked during the Caledonian orogeny, but also involving Caleclonides no basernent lithologies were brought to present exposure levels very thick Neoproterozoic to Lower Palaeozoic sedimentary in North Greenland, and there was no apparent associated magmatism, sequences. The boundaries between the various lithostructural units in the thick-skinned zone are frequently steeply inclined INTRODUCTION thrusts 01' shear zones. Top-to-the west 01' north-west displacement on the thrusts in both the thin- and thick-skinned Two major Palaeozoic orogenie belts are weil preserved in thrust belts probably amounts to two 01' three hundred kilometres Greenland (Fig. I). The 600 km long E-W trending North (HIGGINS & LESLIE 2000). Some thrusts in the thick-skinned Greenland fold belt developed on the site of the Lower Palaeo thrust belt were subsequently reactivated in extension associated zoic Franklinian Basin during the end-Devonian Ellesmerian with orogenie collapse (LARSEN & BENGAARO 1991, ANORESEN orogeny; its continuation is seen to the west in Ellesmere Island et al. 1998). in Arctic Canada. The earlier, N-S trending and 1300 km long East Greenland Caledonides comprises the northern segment of The Caledonian foreland areas fortuitously exposed in windows the Caledonian-Appalachian orogen, and formed by the collision along the margin of the Inland Ice include from south to north of Baltica and Laurentia during the mid-Silurian Scandian (Fig. 2): the Gäseland window, Charcot Land window, Niggli orogeny. The interseetion ofthese two belts is obscured beneath Spids window, Mälebjerg window, Eleonore S0 window, the Mesozoie Wandel Sea B asin offshore eastern North western Dronning Louise Land and the Narreland window. Greenland. The following description of the East Greenland Recognition that the rock successions in the window areas were Caledonides concentrates on the northern segment exposed in all affected to some degree by Caledonian deformation indicates Kronprins Christian Land (Fig. 2). that they should strictly be regarded as parautochthonous rather than autochthonous, with a floor thrust at depth; the limit of This paper gives a brief review of the two Palaeozoic orogenie Caledonian deformation, 01' Caledonian sole thrust, is thus now belts in Greenland which border on the Arctic Ocean, and in placed slightly west of the traditional position, and is largely respect of North Greenland is largely based on existing concealed by the Inland Ice (cf. Figs 1 and 2). The sequences published papers. Description of the East Greenland Caledo exposed in the windows show broad similarities from area to nides incorporates the results of recent Survey mapping area. Tillites of presumed Varanger age occur in the Gäseland, expeditions. Charcot Land and Mälebjerg windows (MONCRIEFF 1989, LESLIE & HIGGINS 1998), quartzites with Skolithos trace fossils m'efound
I Ä.K. Higgins, GeologicaI Survey of Denmark and Greenland, Thoravej 8 DK-2400 in the Mälebjerg and Eleonore S0 windows and in Dronning Copenhagen NV. Denmark.
141 ,'2 Q; .0 :a2 0 E c ro
,'2 Q; .0 :a2 0 E di c .0 ·0 "0 N :2 e c s ro e ·2 Cl. 0 >- "0 c: ro
,'2 '-~ ·in 0 Co
IUJ
Fig. 1: Structural divisions of Greenland, showing the North Greenland (Ellesmerian) fold belt extending into arctic Canada and the circum-Atlantic Caledonian fold belts (after ESCHER & WATT 1976, Fig. I). The traditional west boundary of the Caledonian fold belt in East Greenland shown here follows the allochthonous thrust front (cf. Fig. 2).
142 POST -CAlEDONIAN Paleogene basalts
Paleogene intrusions
Wandel Sea basin: Carboniferous-Paleogene sediments East Greenland basin: Carboniferous-Cretaceous sediments
LATE TO POST-CAlEDONIAN t~:BE::~ Kronprins Christian Land Devonian - continental sediments thin-skinned thrust belt (parautochthonous foreland) CAlEDONIAN FOlD BELT []] Late to post-kinematic granites Neoproterozoic-ordovician sediments (East Greenland) • Neoproterozoic-Silurian sediments (North Greenland)
78' I::::: :1 Palaeo-Mesoproterozoic sediments and basalts ':"-,, (North Greenland)
35' r7;I7l Crystalline complexes ~ (Archaean-Mesoproterozoic)
CAlEDONIAN FORELAND Neoproterozoic-Silurian sediments (North Greenland) Palaeo-Mesoproterozoic sediments and basalts (North and North-East Greenland) Mainly crystalline rocks - parautochthonous windows
Thrust
~ FaultJshear zone
~ Tectonic zone boundaries
74'
Fig. 2: Main geologieal divisions of the East Greenland Caledonides, showing the prineipal teetonie windows, and distinetion of thin- and thiek-skinned thrust belts. Note that interpretation of the windows as mainly parautoehthonous leads 100 km to loeation of the Caledonian sole thrust slightly further west 70' than the traditional limit depictcd in Figure I_ Modified after HIGGINS & LESLIE (2000)_
143 Wandel Sea Basin sequence (post-Caledonian) Lauge Koch Land Fm. (j) LUo Samuelsen Hoj Fm. Z o o Odins Fjord Fm. LU ....J Kap Holbeek Fm. ) Hagen F'jor d Fyns So, Kap Bernhard, Group Campanuladal Fms. Hagen Fjord Gr.) Vandredalen · ' d I thrust Rtvrera a sheat sandstones Independence Fjord Gr. and Zig Zag Dal Basalt Fm. ~~:;t~' Crystalline basement/f~~!j~~~ Vandredalen thrust 25 km Fig. 3: Geologicalmap of Kronprins Christian Land, eastem North Greenland. the norrhemmost segment of the East Greenland CaJedonides. S: Spa-rreglctscher. For age of fonnations see Table I. Cross-section line of Figure 4 is also shown, Modified after HIGGINS & LESLIE (2000). 144 ROBERTSON 1999, HIGGINS et al. in press). and disappears below exposure level along Hekla Sund (Fig. 3). Farther east a broad zone of highly deformed Proterozoic The western marginal zone of the East Greenland Caledonides quartzites and dykes (probably Independence Fjord Group and is only completely exposed in Kronprins Christian Land in Midsommerse dolerites; S0NDERHOLM & JEPSEN 1991; see also eastern North Greenland (Fig. 3; see e.g. HENRIKSEN 1995, 1996, JEPSEN & KALSBEEK 2000, this vol.) extends as far as another RASMUSSEN & SMITH 1996). Here the western foreland, steep N-S trending lineament which approximately marks the undisturbed by Caledonian deformation, preserves a transition between thin-skinned and thick-skinned thrust geo Mesoproterozoic to Early Palaeozoic sedimentary sequence that metry. Crystalline basement rocks east of this lineament and has been related to pre-Iapetan extension, Iapetan rifting and extending to the outer Greenland coast can be interpreted to passive margin sedimentation (Table 1; SMITH et al. 1999). In represent the cores of thick -skinned nappes whose frontal parts an up to 40 km wide parautochthonous fold and thrust belt these would formerly have extended westwards over the thin-skinned same sequences are disrupted by numerous thrusts with thrust belt. Displacement ofthe Independence Fjord Group and generally limited displacements (Fig. 3; HIGGINS & SOPER 1994, associated rocks on the Spserregletscher thrust (Fig. 4), is 1995); total displacement on these thrusts in a cross-section probably more than 50 km, while the displacement of crystalline through this parautochthonous belt along Centrum Sp has been basement rocks on the next thrust to the east may be as much estimated by the authors at about 18 km, assuming the thrusts as 100 km (Fig. 4). to root in flat floor thrusts in Ordovician carbonates. The main nappe front throughout Kronprins Christian Land is formed by Figure 4 also shows the thickness of overburden deduced from the Vandredalen thrust, which transports the Neoproterozoic characteristic colour alteration indices in conodonts extracted siliciclastic rocks known as the Rivieradal sandstones across its from the Lower Palaeozoic carbonates in the parautochthonous rift shoulders (HIGGINS & SOPER 1994, 1995); this thin-skinned belt (J.A. RASMUSSEN and M.P. SMITH personal Neoproterozoic rift sequence is only found in the Vandredalen communications 1998). The calculated overburden increases thrust sheet, and is represented by a hiatus in the foreland. systematically from west to east, reaching approximately 8-10 Uppermost Proterozoic sequences (Hagen Fjord Group) km at the position of the Vandredalen nappe front. It can be overlying the Rivieradal sandstones in the front of the argued that this substantial overburden cannot be due to the Vandredalen thrust sheet are also preserved in the footwall to thickness of the Vandredalen nappe alone, and that higher nappe the Vandredalen thrust and demonstrate a total westward sheets derived from the thick-skinned zone of the Caledonides displacement of about 40 km for the nappe front (22 km on the must once have been present, as surmised above. The timing of Vandredalen thrust and 18 km on the thrusts in the the thrusting in the East Caledonian Caledonides that produced parautochthonous belt to the west; Fig. 4). The allochthonous uplift of the Caledonian mountains is weIl documented (HURST Vandredalen thrust sheet forms the eastern half of the thin et al. 1983, HIGGINS et al. 1991a, 1991b), since it was the erosion skinned thrust belt in Kronprins Christian Land; the flat of the rising mountains that produced the enormous quantities trajectory of the Vandredalen thrust intersecting with the of sediments which from early Late Llandovery times until the topography produces intricate outcrop patterns on the geological Lower Devonian flowed as turbidity currents into the deep-water map (Fig. 3). trough of the Franklinian Basin. Throughout the 600 km length of the Franklinian Basin in North Greenland the commencement The simplified cross-section of Figure 4 illustrates the main of Silurian flysch sedimentation can be dated as Late Llan structure. Eastwards the Vandredalen thrust abruptly steepens, dovery. w E --t..2T ~ Ordovician ~ Crystalline basement 1:::;:::;::1 Independence Fjord Group 1.••..···.··.•..·..:..·.··.··.·,.·1 Rivieradal sandstones Hagen Fjord Group f> "', I :::::::::: & associated volcanics [[[II] ~ -Silurian Fig. 4: Schematic E-W cross-section of the thin-skinned thrust belt in Kronprins Christian Land. The parautochthonous thrust belt referred to in the text is the zone between the sole thrust (ST) and the Vandredalen thrust (VT). SPT is the Spa-rreglerscher thrust. Estimated maximum overburden is from conodont alteration indices (M.P. Smith & lA. Rasmussen, personal communications 1998). See Figure 3 far line of cross-section. Modificd after HIGGINS et al. (in press). 145 STRATIGRAPHY DEPOSITIONAL TECTONIC ENVIRONMENT SETTING thrust loaded Baltica Lauge Koch Land Fm flysch basin collision 5amuelsen H0j Fm Silurian Odins Fjord Fm Turese Fm ßergiurn River Fm thermal subsidence lapetus Sjzelland Fjelde Fm passive Ordovician Wandel Valley Fm block tilting margin Cambrian thermal subsidence Kap Holbeek Fm H extensional lapetus Vendian rifting and opening Hagen block tilting Fjord Group Fyns 50 Fm post-rift thermal Kap Bernhard Fm pre-Iapetus subsidence rift-sag Campanuladal Fm -- - cycle R5 Rivieradal sandstones Riphean extensional rifting (a/lochthonous Vand redalen thrustsheet only) Zig-Zag Dal Basalt Fm ZZ pre-G renville ------intracratonic Independence Fjord Group IF extensional events Tab. I: Proterozoic to Early Palaeozoic stratigraphy of eastern N0l1h Greenland and geotectonic interpretation (modified after SMITH et al. 1999). Caledonian orogenesis and regional metamorphism were exten Greenland fold belt (Fig. 5). This fold belt is characterised by sive, and Caledonian eclogites are recorded emplaced into E-W to ENE-WSW trending fold structures, with deformation crystalline basement gneisses of North-East Greenland (e.g. increasing northwards such that in the extreme north BRUECKNER et al. 1998). Caledonian granites are abundant in the metamorphic grade reaches low amphibolite facies (SOPER & southern half of the East Greenland Caledonides, notably HIGGINS 1987, 1990). In the extreme north there is a north towards the base of the Neoproterozoic Eleonore Bay Super vergent Paleogene overprint associated with the Kap Cannon group, but are not known north of latitude 76 "N; emplacement thrust zone (Eurekan orogcny), but swarms of latc Crctaccous ages of many of the granites, recently determined by SHRIMP dykes (not shown on Fig. 5) provide an easy means of work on zircons and other methods, cluster around 430-420 Ma distinguishing Ellesmerian and Eurekan structurcs. Three (e.g. ANDRESEN et al. 1998, KALSßEEK et al. 1998). Ar-Ar mineral distinct (Ellesmerian) tectonic zones can be recognised, all of cooling ages following the Caledonian metamorphism are in the which appeal' spatially related to the geometry of the Franklinian range 438-370 Ma (Early Silurian - Middle Devonian; e.g. Basin, and are describcd below. DALLMEYER et al. 1994, DALLMEYER & STRACHAN 1994). From earlicst Cambrian to early Silurian time a distinction existed in the Franklinian Basin between the trough, in which NORTH GREENLAND FOLD BELT more than 8 km of turbiditic and hemipelagic sediments were deposited, and the shelf to the south on which accumulated a Sedimentation in the Franklinian Basin was brought to a close thinner carbonate-dominated succession (see also HENRIKSEN & in both Greenland and Arctic Canada by the Ellesmerian HIGGINS this volume). The evolution of the basin has been orogeny, which was the consequence of collision along the north outlined by SURLYK & HURST (1983, 1984), and is presented in margin of the Franklinian Basin with an unknown continent in more detail togcther with the trough and platform stratigraphy the Devonian. In Greenland the Ellesmerian orogenie by HIGGINS et al. (1991 a, 1991b). In summary three stages in the deformation produced the E-W trending 600 km long North evolution of the trough can bc distinguished (SOPER & HIGGINS 146 60 50' 40' ORTHOTECTONIC ZONE - multiphase folding F, originally upright? t ~ F, and F3 north-verging 1 OIVERGENCE & IMBRICATE ZONE Curvilinear thin-skinned structures y In east; west and south verging ~-V 0, strain diminishes 0 westwards, F, 0. FOLOANO THRUST ZONE becomes Thin-skinned south-verging upright structures r ä 1f'00l t~ Eurekan: ~../ Kap Cannon thrust zone (KCTZ) (Tertiary) - - Harder Fjord fault zone (HFFZ) Ellesmerian: ===-= Fold traces (rnid- Palaeozoicl Nansen Land anticlinorium Amundsen Land [:::::.1 WANDEL SEA BASIN ICARB-TERTIARY) ~.~ TROUGH PLATFORM [:.:.:.:••1PE.ARY LAND GP PLATFORM CAMBRa- CARS· _ HAZEN FACIES ~OF:DOVICIAN} ., ONATES82' 1>.. 0::',-,<1 POLKORRIDOREN GP DBUENFM W1WPARADISFJELD GP .PORTFJElD FM .PROTEROZOIC DSKAGENGP. • FORMATIONS o 50 100 150 km ! I I I Fig. 5: Structural map (top) and stratigraphie map (bottom) of the North Greenland fold belt, after SOPER & HIGGINS (1985. Fig. 2). Cross-seetion is shown in Figure 6. The "Hazen facics" of the legend (equivalent to the ...... Hazen Formation of Ellesrnere Island, Canada; TRETTrN et al. 1991) includes the Amundesen Land and Volvedal Groups (trough) and the Kap Stanton Formation (starved platform margin and outer shelf deposits); see -J'.. --.l also HIGGINS et al. (1991'1, b)...... j>.. 00 NORTH KAP KANE F1 folds of orthotectonic zone Harder Fjord fault zone with F2 S2 superimposed Nansen Land anticlinorium "-' HFFZ roots in basin margin faults in footwall of main detachment KTkw - Kap Washington Group volcanics } Wandel 8!fm - Frigg Fjord mudstones (top of (pol) } Deep 8-Sh - Hazen facies } Platform Sik - Lauge Koch Land FormatiOn} Peary K - Cretaceous sediments Sea 8pol - Polkorridoren Group water ~~u ~~~~o~~r~~~~~ates Swl Wulff Land Formation Land CPmm Mallemuk Mountain Formation Basin Cpar - Paradisfjeld Group basin _ - slope Sm - Merquj6q Formation Group Cs - Skagen Group sequence 8po - Portfjeld Formation sequence SOUTH KAP BOPA HANS TAVSEN ISKAPPE Carnbro-Ordovician Lower Silurian platform margin trouqh-platforrn transition (Navarana Fjord lineament) •. 8-Sh ~~~_~ ---7-- ~-~~~_ ---....::::: ...... =------~ NJS & AKH 1985 ------= 5km Limit of mudstone facies in Buen Formation 10 km 5km Fig. 6: North-south cross-section ofthe North Greenland fold bell, after SOPER & HIGGINS (1985, fig. 3). See Figure 5 for line of cross-section. For relationships between deep water and platforrn stratigraphy sec HIGGINS et al. (l991a, b). 1990): aperiod of rapid fault-controlled extension in the early grade rises to low amphibolite facies. In the western part of the Cambrian, during which up to 4 km of turbidites were deposited; orthotectonic zone D 1 has produced spectacular trains of Fl a long period dominated by thermal subsidence in which a folds, upright or slightly northwards verging; D2 strain is weak "starved basin" sequence accumulated; and a second period of and decreases westwards (FRIDERICHSEN & BENGAARD 1985). turbidite deposition in the Silurian when a cumulative thickness of some 5 km was laid down, eventually swamping the shelf. A cross-section through the North Greenland fold belt (Fig. 6) During the early Palaeozoic the trough expanded southwards in illustrates the relationships between the three tectonic zones. several stages by foundering of the platform margin along E Note that in the northernmost part of this cross-section the W trending lineaments which are presumed to have been fault situation is complicated by superimposed Eurekan (Paleogene) controlled (Surlyk & Hurst 1983, 1984); the most important of deformation with north-directed displacements on the south these is the Navarana Fjord lineament or escarpment (Fig. 5) dipping thrusts of the Kap Cannon thrust zone. which formed the platform margin in early Silurian time. In North Greenland crystalline basement rocks are exposed only A southern thin-skinned fold and thrust zone coincides with a locally in the southern foreland at the margin of the Inland Ice. region which was transitional between the platform and the trough Evidence that the Franklinian Basin developed above for much of the Cambrian (Fig. 5). Folds verge southwards, and continental ernst is seen in the occurrence of crystalline xenoliths thrusts dip at gentle to moderate inclinations northwards and have in end-Cretaceous to Paleogene dykes and volcanic plugs related a southwards sense of displacement. Major fold traces and linear to the Eurekan orogeny. Interpretative cross-sections of the steep belts trend parallel to the slightly curved Navarana Fjord southern margin of the North Greenland fold belt (SOPER & escarpment and exhibit the same arcuate trends between E-Wand HIGGINS 1990) demonstrate that some of the extensional faults ENE-WSW. Clearly the early Silurian facies boundary which governed sedimentation in the Franklinian Basin were represented by the Navarana Fjord escarpment constrained the reactivated as thrusts during the Ellesmerian orogeny (Fig. 7); pattern of deformation which developed in the trough sediments displacements on these reactivated structures was modest, ofthe as they were compressed against the platform margin. order of a few kilometres, and directed southwards, but was insufficient to bring basement lithologies to present exposure The divergence and imbricate zone (Fig. 5) corresponds with a levels on Ellesmerian thrusts. tract across which the vergence of folds changes from south to north. It also coincides with a profound change in the strati graphie level of rocks exposed at the present surface; to the north INTERSECTION OF THE ELLESMERlAN AND CALE in the orthotectonic zone on the site of the former deep-water DONIAN FOLD BELTS trough Lower Cambrian rocks are exposed, while to the south Silurian rocks are exposed except where older rocks are brought The assumed interseetion ofthe North Greenland (Ellesmerian) to the surface in anticlinal fold cores and thrust sheets. The fold belt and the East Greenland Caledonides is obscured divergence zone widens eastwards, where it is characterised by beneath post-Ellesrnerian sedimentary successions offshore imbricate thrusts with curvilinear traces which verge to the west eastern North Greenland. These Carboniferous to Paleogene and south (HÄKANSON & PEDERSEN 1982, PEDERSEN 1986). SOPER successions are known as the Wandel Sea Basin (e.g. STEMMERIK & HIGGINS (1985) viewed the imbricate thrusts as an integral part & HÄKANSON 1991, HÄKANSSON et al. 1991, HÄKANSSON & of the Ellesmerian North Greenland fold belt, and attributed their STEMIvJERIK 1984, 1989), and onshore are seen to be disturbed arcuate trends to bending of south-verging thrusts as they by Eurekan (Paleogene) deformation related to the Wandel Hav impinged obliquely against the buried Navara Fjord escarpment; strike slip mobile belt (HÄKANSSON & PEDERSEN 1982), one of alternative interpretations of this curvilinear imbricate thrust the major fracture zones in North Greenland associated with the zone are given by SURLYK & HURST (1984) and PEDERSEN (1986). opening of the North Atlantic Ocean. There is little evidence In the extreme east the divergence and imbricate zone appears onshore to indicate the nature of the interseetion of the two fold to be truncated by the Harder Fjord fault zone (Fig. 5). belts, although there is a marked change in strike of the margi nal thrust systems of the extreme northernmost seetion of the The northernmost orthotectonic zone developed on the site of East Greenland Caledonides in northern Kronprins Christian the deep water trough of the Franklinian Basin, with its thick Land. There the regional N-S trending strikes swing to NNE fill of Lower Cambrian calcareous and siliciclastic turbidites. In SSW and to almost NE-SW trends where last seen, as the fold the eastern part of this zone structures are all broadly E-W belt plunges beneath the later Wandel Sea Basin sediments (Fig. trending, again essentially parallel to the Navarana Fjord 3). The hidden continuation may even continue this swing such escarpment, except in the extreme east where the Harder Fjord that the Caledonian orogenie trends become sub-parallel to the fault zone (HFFZ, Fig. 5) truncates the southern two zones; the later Ellesmerian trends of the North Greenland fold belt. strnctures are referable to three, coaxial tectonic episodes (SOPER & HIGGINS 1985, 1987). Fl folds are dominant in the south where they are upright. To the north F2 folds become superimposed ACKNOWLEDGMENTS on Fl and are consistently overturned northwards. Near the north coast of Greenland Fl and F2 are isoclinal, third folds This paper is published with the permission of the Geological appear superimposed on the S2 schistosity and the metamorphie Survey of Denmark and Greenland. 149 >-' U1 o WULFF LAND ANTIClINE NORTH SOUTH Cbu ~~{!\,,~: Chester Bierg Fm. Shb Skagen Ge. Sik ...... Sm. crystalline basement Navarana Fjord escarpment Opo ....;. WULFF LAND ./ crystalline basement restored section SiL carbonates Merqujoq Fm. {; - 0 carbonates / / Hazen Fm. /~ r- Buen Fm. --- Portfjeld Fm. Buen Fm. ----~------Portfjeld Fm. (. ~ '" Skagen Gp. ~-/-- , -----~~.------'" ~~~- ---..;./( "..~./ '" ~... -.. -- ,~j//~;;. /' Sik Lauge Koch Land Fm. / //' Shb Hand Bugt Mem. / /'./' C-Ohz Hazen Fm. / / Okm 5 km 10 km Csk Skagen Gp. / / I [ I[ Cpo Portfjetd Fm. / / Cbu Buen Fm. / / / // /// /: / Fig. 7: Interpretative dcep section through the marginal fold and thrust zone of the North Greenland fold belt in Wulff Land, with restored seetion bclow. Illustrates reactivation of extensional faults during sedimentation as thrusts during Ellesmerian compression. After SOPER & HIGGINS (1990, Fig. 7). The 'crystalline basernent' underying the basin may include Proterozoic rift-related sediments. References Jepsen, HF & Kalsbeek, F (this volume): Preeambrian evolution ofNorth anel Nonh-East Greenlanel: erystalline basemcnt anelseelimentary basins.- Polar Andresen. A., Hartz; E.H & Vold, .1. (1998): A late orogenie extensional origin forschung. for the infraerustal gneiss domes of the East Greenland Caledonides (72 Kalsbeek, F, Nutman. A.P. & Taylor; P.N (1993): Palaeoproterozoie basement 74 °N)._ Teetonophysies 285: 353-369. provinee in the Caleelonian folel belt of North-East Greenlanel.- Preeambr. Brueckner; HK., Gilotti, J.A. & Nutman. A.P. (1998): Caledonian eclogire-facies Res. 63: 163-178. metamorphism of Early Proterozoie protoliths from the North-East Kalsbeek, F, Nutman. A.P. & Jepsen, F (1998): Granites in the Caleelonian folel Greenland eelogite provinee.- Contrib. Miner. Petr. 130: 103-120. belt, East Greenlanel.- In: K.S. FREDERIKSEN & K. THRANE (eels.) Dallmeyer; R.D. & Strachan, R.A. (1994): 4°ARjJ9Ar mineral age eonstraints on Symposium on Caleelonian geology in East Greenlanel. Abstract Vo!. Dan the timing of deformation and metamorphisrn, North-East Greenland marks og Gronlands Geo!. Unelers. Rapp. 1998/46: 43-44. Caledonides.- In: A.K. HIGGINS (cd.) Geology of North-East Greenland, Larsen, PH & Bengaard, HJ. (1991): Devonian basin initiation in East Rapp. Gronlands Geo!. Undcrs. 162: 153-162. Greenlanel: a result of sinistral wreneh faulting anelCaleelonian extensional Dallmeyei; R.D., Strachan, R.A. & Henriksen, N (1994): 4°ArjJ9Ar mineral age eollapse.- J. Geo!. Soe. Lonelon 148: 355-368. reeord in NE Greenland: implications for teetonie evolution of the North Leslie, A.G. & Higgins, AK. (1998): On the Caleelonian geology of Andree Lanel, Atlantie Caledonides.- 1. Geo!. Soe. 151: 615-628. Eleonore S0 anel aeljaeent nunataks, East Greenlanel.- In: A.K. HIGGINS Escher, A. & Watt, H~S. (eds.) (1976): Geology of Greenland, 603 pp. & K.S. FREDERIKSEN (eels.), Caleelonian Geology of East Greenlanel Copenhagen: Geologieal Survey of Greenland. 72°-74 ON: preliminary reports frorn the 1997 expeelition. Danmarks og Granlands Geol, Unelers. Rapp. 1998128: 11-27. Friderichsen, J.D. & Bengaard, HiJ. (1985): The North Greenland fold belt in eastern Nansen Land.- Rapp. Granlands Geo!. Undcrs. 126: 79-86. Moncrieff, A.C.M. (1989): The Tillite Group anelrelateel rocks of East Greenlanel: implications for Late Proterozoie palaeogeography.- In: R.A. GAYER (eel.) Häkansson, E & Pedersen, SAS. (1982): Late Paleozoie to Tertiary evolution The Caleeloniele Geology of Seandinavia, 285-297. Lonelon: Graharn & of the eontinental margin in North Greenland.- In: A.F. EMBRY & H.R Trotman. BALKWILL (eds.) Aretic Geology and Geophysics, Mem. Canadian Soe. Petro!' Geo!. 8: 331-348. Pedersen, S.A.S. (1986): A transverse, thin-skinncd, thrust belt in the Paleozoic North Greenlanel folel belt.- Bull. Geo!. Soc. Amer. 97: 1442-1455. Hdkansson, E. & Stemmerik, L. (1984): Wandel Sea Basin - The North Greenlanel equivalent to Svalbard and the Barents Shelf.- In: A.M. Rasmussen. J.A. & Smith, M.P. (1996): Lower Palaeozoie carbonates in castern SPENCER et a!. (eds.) Petroleum geology of the North European margin, North Greenlanel, anel the demise of the 'Srefaxi Elv nappe'.- Bull. 97-107. London: Graham & Trotman for the Norwegian Petroleum Soeiety. Gronlands Geo!. Undcrs. 172: 49-54. Häkansson, E & Stemmerik, L. (1989): Wanelel Sea Basin- a new synthesis of Smith, MP. & Robertson, S. (1999): Venelian - Lower Palaeozoic stratigraphy the late Paleozoie to Tertiary accumulation in North Greenlanel.- Geology of the parantochthon in the Mälebjerg anelElconore S0 thrust windows, East 17: 683-686. Greenland Caleelonieles.- In: A.K. HIGGINS & K.S. FREDERIKSEN (eels.), Geology of East Greenland 72-75 ON, mainly Caleelonian: Hdkansson, E, Heinberg. C. & Stenunerik, L. (1991): Mesozoie and Cenozoie preliminary reports from the 1998 expeelition. Danmarks og Gronlands history of the Wandel Sea Basin arca, North Greenland.- Bull. Granlands Geol, Unelers. Rapp. 1999/19: 169-182 Geo!. Undcrs. 160: 153-164. Smith, M.P, Soper; Ni., Higgins, A.K., Rasmussen, JA & Craig, L.E. (1999): Henriksen, N (1995): Eastern North Greenland, the I : 500000 mapping Palaeokarst systems in the Proterozoic of eastern North Greenlanel project.- Rapp. Gronlands Geo!. Unelers. 165: 53-58. implications for Proterozoie - Early Palaeozoic basin elevelopment anel Henriksen, N (1996): Conclusion of the 1 : 500 000 field mapping in eastern tectonic history.- J. Geol. Soc. Lonelon 156: 113-124. North Greenland.- Bull. Gronlands Geo!. Undcrs. 172: 42-48. Sonderholm. M & Jepsen, HF (1991): Proterozoic basins ofNorth Greenlanel. Henriksen, N & Hi ggin s, A.K. (this volume): Early Palaeozoie basin Bull. Gronlands Geo!. Unelers. 160: 49-69. devclopmcnt of North Greenland - part of the Franklinian Basin.- Polar Soper; NJ. & Higgins, A.K. (1985): Thin-skinncd struetures at the trough forschung. platform transition in North Greenlanel.- Rapp. Gronlands Geo!. Unelers. Higgins A.K. & Leslie, AG. (2000): Restoring thrusting in the East Greenlanel 126: 87-94. Caleelonieles.- Geology 28: 1019-1022. Soper; NJ. & Higgins, A.K. (1987): A shallow detachment beneath the North Higgins, A.K. & Soper; NJ. (1994): The Caledonian thrust belt of Kronprins Greenlanel folel bell: implications for sedimentation anel tectonics.- Geol. Christian Land.- In: N. HENRIKSEN (ed.) Express Report, Eastern North Mag. 124: 441-450. Greenland and Nonh-East Greenland 1994: 57-67. Copenhagen: Granlands Soper; NJ. & Higgins, A.K. (1990): Moelels for the Ellesmerian mountain front Geo!. Undcrs. in North Greenlanel: a basin margin inverteel by basement uplift.- J. Struct. Hi ggins, A.K. & Soper. Ni. 1995: Teetonie and other observations in Geo!. 12: 83-97. Vandreelalen and adjaeent areas of Kronprins Christian Land.- In: A.K. Stemmerik, L. & Häkansson. E (1991): Carboniferous anel Permian history of HIGGINS (ed.) Express Report, Eastern North Greenland anel North-East the Wanelel Sea Basin, North Greenlanel.- Bull. Granlands Geo!. Unelers. Greenland 1995: 105-114. Copenhagen: Gronlands Geo!. Unders. 160: 141-151. Higgins, A.K., lneson, J.R., Peel, J.S., Surlvk, F & Sonderholm. M. (199Ia): Strachan, RA, Friderichsen, J.D., Holdsworth, R.E & .lcpsen, HF (1994): Lower Palaeozoic Franklinian Basin ofNorth Greenland.- Bull. Granlands Regional geology anel Caleelonian structurc, Dronning Louise Land, North Geo!. Unelers. 160: 71-139. East Greenlanel.- In: A.K. HIGGINS (ed.), Geology of North-East Higgins, A.K., Ineson, J.R., Peel, .l.S., Surlyk, F & Sonderholm. M. (1991 b): Greenlanel. Rapp. Gronlands Geo!. Unelers. 162: 71-76. Cambrian to Silurian basin development and sedimentation, North Surlyk, F & Hurst, .I.M. (1983): Evolution of the early Palaeozoic deep-water Greenland.- In: H.P. TRETTIN (ed.), Geology of the Innuitian orogen anel basin of North Greenlanel- aulacogen 01' narrow ocean?- Geology 11: 77 aretie platform of Canada and Greenland, 111-161. Geology of Canada 3, 81. Chapter 7 (also Geology of North America, E). Calgary: Geol. Surv. Ca naela. Surlyk F & Hurst, .I.M. (1984): The evolution ofthe early Palaeozoic dcep-water basin of North Greenlanel.- BuH. Gcol. Soc. Amer. 95: 131-154. Higgins, A.K., Leslie, AG. & Smith M.P. (in press): Neoproterozic - Lower Palaeozoic stratigraphreal relationships in the marginal thin-skinned thrust Trettin, HP. (ed.) 1991: Geology of the Innuitian orogen anel aretie platform of belt of the East Greenlanel Caledonides: comparisons with the foreland in Canaela anel Greenlanel.- Geology of Canaela 3: 569 pp. (also Geology of Seotland.- Geo!. Mag. North America, E). Calgary: Geological Survey of Canaela. Hurst, J.M, McKcrrow; WS., SOpeJ; NJ. & Surlvk, F (1983): The relationship between Caleelonian nappe tectonics anel Silurian turbielite eleposition in North Greenlanel.- J. Geo!. Soe. Lonelon 140: 123-132. 151