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The Lyngen Magmatic Complex ophiolite: preservation of pre- and syn-collisional structures and implications for the nappe thrusting sequence in the Northern Norwegian Caledonides.

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Title: The Lyngen Magmatic Complex ophiolite: preservation of pre- and syn-collisional structures and implications for the nappe thrusting sequence in the Northern Norwegian Caledonides.
Authors: Galindos-Alfarache, Marina1 (AUTHOR) marina.galindos@uit.no, Stünitz, Holger1,2 (AUTHOR), Soret, Mathieu2,3 (AUTHOR), Bonnet, Guillaume4 (AUTHOR), Dubacq, Benoît5 (AUTHOR), Ganerød, Morgan6 (AUTHOR)
Source: Tectonophysics. May2025, Vol. 904, pN.PAG-N.PAG. 1p.
Subjects: Shear zones, Mafic rocks, Analytical geochemistry, Phase equilibrium, Raman spectroscopy
Abstract: The Lyngen Magmatic Complex (Northern Norway) marks a major discontinuity in the metamorphic gradient of the North Norwegian Caledonides nappe sequence. The Lyngen Magmatic Complex preserves pre- and syn -collisional structures and parageneses of the Caledonian orogeny. This study differentiates the two deformation events and offers a tectono-metamorphic model for the region, using a combination of field-based data, geochemical analysis, radiochronometric dating, and thermodynamic modelling. It is demonstrated that the precollisional event (D1) developed in a dextral strike-slip transpressional regime, generating N S-trending subvertical shear zones with subhorizontal shear displacement and steeply inclined isoclinal folding. The D1 metamorphic fabrics developed at 486 ± 9 Ma on a retrograde temperature-path, from amphibolite (680 800 °C, 0.5 0.9 GPa) to greenschist facies (300 450 °C, 0.3 0.75 GPa) conditions. The subsequent syn -collisional event (D2) produced a subhorizontal foliation, top-to-SE-directed thrust deformation at the base of the Lyngen Magmatic Complex. D2 rock fabrics represent typical nappe stacking structures during the Scandian collisional stage (∼430 Ma). The vertical D1 structures are overprinted by D2 fabrics in the thrust contact region only. Mineral assemblages crystallizing during D2 indicate a transition from lower amphibolite to greenschist conditions. Thermobarometry suggests significant re-heating after D1, with D2 maximum conditions ∼650 °C and 1.1 GPa at the base of the Lyngen Magmatic Complex and ∼558 610 °C and 0.8 1.3 GPa for the underlying graphite-bearing metasediments. Argon dating and the temperature difference between the Lyngen Magmatic Complex and the underlying units testify to out-of-sequence thrusting at 426 ± 7.5 Ma at the base of the Lyngen Magmatic Complex. The present results constrain the localization of the oceanic units of the North Norwegian Caledonides outboard and to the North of their present position. Consequently, stacking of uppermost units (likely of Laurentian origin) on top of the Lyngen Magmatic Complex occurred before their final emplacement onto the Reisa Nappe Complex (probably mostly Baltica-derived). • The LMC shows a polymetamorphic history with two deformation events at 486 ± 9 and ∼ 430 Ma (Scandian event). • The Eidnas Formation only records prograde metamorphism with temperatures between 558− 610 ± 10 °C and pressures of 0.8−1.3 GPa. • P-T distribution shows out-of-sequence thrusting below the LMC and the Eidnas Formation between 425 ± 5 Ma and 427 ± 10 Ma. • Strain localization and partitioning in mafic rocks control and limit the structural and metamorphic overprint. [ABSTRACT FROM AUTHOR]
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Abstract:The Lyngen Magmatic Complex (Northern Norway) marks a major discontinuity in the metamorphic gradient of the North Norwegian Caledonides nappe sequence. The Lyngen Magmatic Complex preserves pre- and syn -collisional structures and parageneses of the Caledonian orogeny. This study differentiates the two deformation events and offers a tectono-metamorphic model for the region, using a combination of field-based data, geochemical analysis, radiochronometric dating, and thermodynamic modelling. It is demonstrated that the precollisional event (D1) developed in a dextral strike-slip transpressional regime, generating N S-trending subvertical shear zones with subhorizontal shear displacement and steeply inclined isoclinal folding. The D1 metamorphic fabrics developed at 486 ± 9 Ma on a retrograde temperature-path, from amphibolite (680 800 °C, 0.5 0.9 GPa) to greenschist facies (300 450 °C, 0.3 0.75 GPa) conditions. The subsequent syn -collisional event (D2) produced a subhorizontal foliation, top-to-SE-directed thrust deformation at the base of the Lyngen Magmatic Complex. D2 rock fabrics represent typical nappe stacking structures during the Scandian collisional stage (∼430 Ma). The vertical D1 structures are overprinted by D2 fabrics in the thrust contact region only. Mineral assemblages crystallizing during D2 indicate a transition from lower amphibolite to greenschist conditions. Thermobarometry suggests significant re-heating after D1, with D2 maximum conditions ∼650 °C and 1.1 GPa at the base of the Lyngen Magmatic Complex and ∼558 610 °C and 0.8 1.3 GPa for the underlying graphite-bearing metasediments. Argon dating and the temperature difference between the Lyngen Magmatic Complex and the underlying units testify to out-of-sequence thrusting at 426 ± 7.5 Ma at the base of the Lyngen Magmatic Complex. The present results constrain the localization of the oceanic units of the North Norwegian Caledonides outboard and to the North of their present position. Consequently, stacking of uppermost units (likely of Laurentian origin) on top of the Lyngen Magmatic Complex occurred before their final emplacement onto the Reisa Nappe Complex (probably mostly Baltica-derived). • The LMC shows a polymetamorphic history with two deformation events at 486 ± 9 and ∼ 430 Ma (Scandian event). • The Eidnas Formation only records prograde metamorphism with temperatures between 558− 610 ± 10 °C and pressures of 0.8−1.3 GPa. • P-T distribution shows out-of-sequence thrusting below the LMC and the Eidnas Formation between 425 ± 5 Ma and 427 ± 10 Ma. • Strain localization and partitioning in mafic rocks control and limit the structural and metamorphic overprint. [ABSTRACT FROM AUTHOR]
ISSN:00401951
DOI:10.1016/j.tecto.2025.230706