Lomier Complex
Stratigraphic label: [ppro]lom
Map symbol: pPlom

First published: 18 April 2018
Last modified: 7 October 2022











  DISCLAIMER: This English version is translated from the original French. In case of any discrepancy, the French version shall prevail.  

Informal subdivision(s)
Numbering does not necessarily reflect the stratigraphic position.
pPlom2 Banded gneiss with alternating diorite and granite
pPlom1 Hypersthene gneiss
pPlom1b Charnockitic gneiss
pPlom1a Enderbitic gneiss
Author(s): Girard, 1990
Age: Paleoproterozoic
Stratotype: None
Type area: Lac Courdon area (NTS sheet 14E12)
Geological province: Churchill Province
Geological subdivision: Falcoz Lithotectonic Domain
Lithology: Hypersthene gneiss
Category: Lithodemic
Rank: Complex
Status: Formal
Use: Acive




The Lomier Complex was defined by Girard (1990) in the Lac Courdon area (NTS sheet 14E12). It consists of hypersthene gneisses of various compositions characterized by a strong aeromagnetic signature and a N-S tectonic grain along the Québec-Labrador border. This complex has also been described in the Lac Henrietta area (Lafrance et al., 2015) and extended northward in the Koroc River and Hébron area (Verpaelst et al., 2000) and in the Point le Droit area (Mathieu et al., 2018), where it pinches on the Abloviak Shear Zone (ZCabl) that shifts to the WNW in this area.

In the Koroc River and Hébron area, Verpaelst et al. (2000) had grouped units from the Courdon and Koroc River suites within undifferentiated units of the Lomier Complex. As part of a synthesis of the southeastern Churchill Province (Lafrance et al., 2018), units were standardized across the Falcoz Lithotectonic Domain (Lafrance and Vanier, 2022). The table below summarizes the equivalences between the current and previous units.



Revised Units and Subunits (Mathieu et al., 2018; Lafrance and Vanier, 2022)

Previous Units and Subunits




Lafrance et al., 2015

pPlom1 (in part)

Verpaelst et al., 2000



Lafrance et al., 2015


Girard, 1990



Lafrance et al., 2015


Girard, 1990



Lafrance et al., 2015


Girard, 1990






The Lomier Complex consists of two closely related packages in the field: a supracrustal sequence, attached to the Koroc River Suite, which is intersected by the Courdon Intrusive Suite. Girard (1990) grouped rocks whose protoliths are no longer recognizable due to their heterogeneity, as well as those that have developed intense tectonic banding in gneiss units of the Lomier Complex (pPlom). This author considers rocks of the Courdon Intrusive Suite and the Koroc River Suite to be the protoliths of these gneisses. The Lomier Complex consists of two units: a hypersthene gneiss unit (pPlom1) and a banded gneiss unit with alternating diorite and granite (pPlom2).



Lomier Complex 1 (pPlom1): Hypersthene Gneiss

Gneisses of the Lomier Complex are considered to be alternating millimetric to decametric horizons of Koroc River Suite and Courdon Intrusive Suite rocks in deformation zones. They usually contain decimetric horizons that are better preserved and in gradual contact with these units. Overall, the gneisses show a well-developed foliation and lineation, commonly mylonitic with quartz bands and rods. According to Girard (1990), gneiss represents zones of mixing between different pretectonic to syntectonic lithologies. The enderbite protolith dominates (60%) and is intertwined with amphibolite (30%) and paragneiss (10%). Banding occurs at all scales, from decametre to millimetre, with bands continuous hectometrically or in regular or heterogeneous klippes. Contacts are paralleled and transposed into foliation. The mineralogy of the gneisses is similar to that of their protoliths (Courdon Intrusive Suite and Koroc River Suite).

Gneisses of the Lomier Complex has sharp banding with alternating millimetric to decamatric bands and horizons of enderbite, diorite, charnockite and opdalite. All of these phases are fine to very fine grained and highly magnetic. Rocks are affected by a reduction in grain size of variable intensity, marked by fine-grained corridors between quartzofeldspathic porphyroclasts (Charette and Guilmette, 2014). Mineral phases have undulatory extinction, deformed twins, and indented crystalline edges, indicating intense deformation. Gneissosity is defined by the concentration of orthopyroxene in laminae and the presence of quartz bands with subgrain extinction. Locally, it was possible to distinguish predominantly enderbitic (pPlom1a) or predominantly charnockitic (pPlom1b) gneiss.



Lomier Complex 1a (pPlom1a): Enderbitic gneiss

Subunit pPlom1a is characterized by the dominance of enderbitic horizons in gneiss (50-65%). These greenish or brown sugar coloured leucocratic horizons contain 5 to 12% orthopyroxene. Gneiss also comprises 20 to 35% intermediate and mafic horizons (hypersthene diorite and gabbronorite), generally slightly finer than felsic horizons. These contain 35 to 55% ferromagnesian minerals, dominated by orthopyroxene and clinopyroxene. Enderbitic gneiss also contains diffuse centimetric bands of slightly coarser-grained enderbite and charnockite, which could represent leucosome. Accessory minerals observed in the different phases of the gneiss are apatite, zircon, opaque minerals and epidote. Orthopyroxene is variably retrograded to hornblende and biotite.



Lomier Complex 1b (pPlom1b): Charnockitic gneiss

The charnockitic gneiss is light brown sugar and contains 4 to 10% ferromagnesian minerals, mainly pyroxenes. Stretching of minerals is generally more developed than banding and foliation. Banding, which is hardly visible in outcrop, is marked by the variation of the percentage of K-feldspar (charnockite to opdalite) and in grain size (very fine to fine), which can be easily observed on stained samples. Between 5% and 15% diffuse bands or intrusions of leucocratic and coarse-grained charnockite are paralleled in deformation. K-feldspar is perthitic and commonly rimmed with myrmekites. Ferromagnesian minerals of charnockitic gneiss are dominated by broken orthopyroxene, not altered or partially replaced by a mixture of iddingiste and carbonates. The gneiss also contains thin biotite flakes and up to 2% finely disseminated magnetite. The main accessory minerals are apatite, zircon, amphibole (replacing pyroxene) and interstitial carbonates. Clinopyroxene and garnet are also observed sporadically.



Lomier Complex 2 (pPlom2): Banded gneiss with alternating diorite and granite

The granitic gneiss unit forms a 3 to 5 km wide strip on the western edge of the Lomier Complex and probably represents an area of retrograde metamorphism linked to the Lac Pilliamet Shear Zone (ZCpil). This unit consists of two deformed alternating phases in decimetric to metric horizons: a dioritic grey phase (locally granitic) and a coarser-grained pink granite phase. The granitic phase is generally dominant. The diorite is granoblastic and contains between 15 and 35% ferromagnesian minerals, consisting of green hornblende and chloritized brown biotite. Pink granite is hololeucocratic, not granoblastic. It is slightly foliated to ultramylonitic and hematitized along faults. According to Girard (1990), the granitic phase represents veins and lenses of leucosome with sharp contacts with gneiss (paleosome). A thin biotitic melanosome locally forms a millimetric rim at the interface between granite and host gneiss. The granite is dominated by partially recrystallized microcline-rich lenses alternating with quartz bands with undulatory extinction. It contains a lesser amount of biotite, brown or green, with zircon and opaque inclusions, as well as muscovite and chlorite.


Thickness and Distribution

The Lomier Complex is a 10 to 15 km wide N-S strip spanning more than 200 km long along the Québec-Labrador border. It is limited by the ZCpil to the west and the ZCabl to the east. In the northern part of the Falcoz Lithotectonic Domain, the ZCpil converges with the ZCabl, which then branches off to the west-northwest in this area. The Lomier Complex then occurs at the junction of the two shear zones. Only a few bands of supracrustal rocks assigned to the Koroc River Suite are present in the ZCabl at the northern end of the Falcoz Domain. The gneiss units cover an area of ~772 km2 within the Falcoz Domain. Specifically, units pPlom1 and pPlom2 occupy ~274 km2 and ~238 km2 respectively, while subunits pPlom1a and pPlom1b cover an area of ~130 km2 each.



An age of ~1877 Ma was obtained in Labrador from an enderbitic gneiss located at the eastern edge of the Lomier Complex (Bertrand et al., 1993). Inherited ages obtained in a sample from a gneiss located within the ZCabl (outcrop 2017-JV-2140) are similar to those obtained from detrital zircons in a paragneiss from the Koroc River Suite (2447-2039 Ma; Charette et al., 2021), suggesting that the sample analyzed would be a gneiss of sedimentary origin. The metamorphic age around 1930 Ma is interpreted to be that of the metamorphic episode that initiated gneiss formation (David, 2020).



Unit Sample Number Isotopic System Mineral Crystallization Age (Ma) (+) (-) Inherited Age (Ma) (+) (-) Metamorphic Age (Ma) (+) (-) Reference(s)
pPlom1a ET 89-023 U-Pb Zircon 1876.9 1 1       1822.5 1.1 1.1 Bertrand et al., 1993
pPlom1 2017-JV-2140A U-Pb Zircon       2179 14 14 1930.1 9.2 9.2 David, 2020
2266 18 18 1844.5 8.9 8.9
2375 12 12      
2488 15 15      

Stratigraphic Relationship(s)

The ZCpil juxtaposes the Lomier Complex and the Sukaliuk Complex located to the west. On the east side, the ZCabl represents the contact between the Lomier and Tasiuyak complexes.

The transitional and diffuse contact between the rocks of the Courdon and Koroc River suites and the gneisses of the Lomier Complex led Girard (1990) to consider that the gneisses represent more deformed zones of these two suites.

The origin of the Lomier Complex remains unknown at this time (Wardle et al., 1990 and 2002; Lafrance et al., 2016; Corrigan et al., 2018; Charette et al., 2021), which represents a significant gap in the geodynamic evolution of the region (Charette, 2016). It could be an equivalent of the Cumberland Batholith on Baffin Island (St-Onge et al., 2009; Wardle et al., 2002) and thus be interpreted as the root of a magmatic arc emplaced at the eastern margin of the Falcoz Lithotectonic Domain (Ermanovics and Van Kranendonk, 1998). However, the most accepted hypothesis is that it is a continental arc related to eastward subduction of the Falcoz Lithotectonic Domain beneath the Nain Province (Van Kranendonk and Wardle, 1996; Wardle et al., 2002).




Does not apply.




Publications Available through SIGÉOM Examine



DAVID, J., 2020. Datations U-Pb dans les provinces du Supérieur et de Churchill effectuées au GEOTOP en 2018-2019. MERN, GEOTOP; MB 2020-01, 30 pages.



LAFRANCE, I., BANDYAYERA, D., CHARETTE, B., BILODEAU, C., DAVID, J., 2016. Géologie de la région du lac Brisson (SNRC 24A). MERN; RG 2015-05, 64 pages, 1 plan.

LAFRANCE, I., CHARETTE, B., VANIER, M.-A., 2018. Sud-est de la Province de Churchill, Nunavik, Québec, Canada: synthèse de la géologie. MERN; BG 2018-12

LAFRANCE, I., VANIER, M.-A., 2022. Domaine lithotectonique de Falcoz, sud-est de la Province de Churchill, Nunavik, Québec, Canada : synthèse de la géologie. MERN; BG 2022-01, 2 plans.

MATHIEU, G., LAFRANCE, I., VANIER, M.-A., 2018. Géologie de la région de pointe Le Droit, Province de Nain et sud-est de la Province de Churchill, Nunavik, Québec, Canada. MERN; BG 2018-07, 4 plans.

VERPAELST, P., BRISEBOIS, D., PERREAULT, S., SHARMA, K. N. M., DAVID, J., 2000. Géologie de la région de la rivière Koroc et d’une partie de la région de Hébron, 24I et 14L. MRN; RG 99-08, 62 pages, 10 plans.


Other Publications

BERTRAND, J.M., RODDICK, J.C., VAN KRANENDONK, M.J., ERMANOVICS, I., 1993. U-Pb geochronology of deformation and metamorphism across a central transect of the Early Proterozoic Torngat Orogen, North River map area, Labrador. Canadian Journal of Earth Sciences; volume 30, pages 1470-1489.

CHARETTE, B. 2016. Long-lived anatexis in the exhumed middle crust from the Torngat Orogen and Eastern Core Zone: Constraints from geochronology, petrochronology, and phase equilibria modeling. University of Waterloo; thèse de maîtrise, .

CHARETTE, B., GODET, A., GUILMETTE, C., DAVIS, D.W., VERVOORT, J., KENDALL, B., LAFRANCE, I., BANDYAYERA, D., YAKYMCHUK, C., 2021. Long-lived anatexis in the exhumed middle crust of the Torngat Orogen: Constraints from phase equilibria modeling and garnet, zircon, and monazite geochronology. Lithos; volume 388-389. 2021.106022

CORRIGAN, D., WODICKA, N., McFARLANE, C., LAFRANCE, I., VAN ROOYEN, D., BANDYAYERA, D., BILODEAU, C. 2018. Lithotectonic framework of the Core Zone, Southeastern Churchill Province. Geoscience Canada; volume 45, pages 1-24.

ERMANOVICS, I., VAN KRANENDONK, M., 1998. Geology of the Archean Nain Province and Paleoproterozoic Torngat Orogen in a transect of the North River-Nutak map areas, Newfoundland (Labrador) and Quebec. Geological Survey of Canada; volume 497, pages 1-156.

ST-ONGE, M.R., VAN GOOL, J. A.M., GARDE, A., SCOTT, D.J., 2009. Correlation of Archaean and Palaeoproterozoic units between northeastern Canada and western Greenland: constraining the pre-collisional upper plate accretionary history of the Trans-Hudson orogen. Geological Society, London; Special Publications, vol. 318, pages 193-235.

VAN KRANENDONK, M.J., WARDLE, R.J., 1996. Burwell domain of the Palaeproterozoic Torngat Orogen, northeastern Canada: tilted cross-section of a magmatic arc caught between a rock and a hard place. In: Precambrian Crustal Evolution in the North Atlantic Region (Brewer, T.S., editor). The Geological Society, London; Geological Society Special Publication No. 112, pages 91-115.

WARDLE, R.J., RYAN, B., NUNN, G.A.G., MENGEL, F.C., 1990. Labrador segment of the Trans-Hudson Orogen: crustal development through oblique convergence and collision. In: The Early Proterozoic Trans-Hudson Orogen of North America (Lewry, J.F. and Stauffer, M.R., editors). Geological Association of Canada; Special Paper 37, pages 353-369.

WARDLE, R.J., JAMES, D.T., SCOTT, D.J., HALL, J., 2002. The southeastern Churchill Province: synthesis of a Paleoproterozoic transpressional orogen. Canadian Journal of Earth Science; volume 39, pages 639-663.


Suggested Citation

Ministère de l’Énergie et des Ressources naturelles (MERN). Lomier Complex. Quebec Stratigraphic Lexicon. [accessed on Day Month Year].


First Publication

Isabelle Lafrance, P. Geo., M.Sc. (redaction)

Mehdi A. Guemache, P. Geo., Ph.D. (coordination); Pierre Lacoste, P. Geo., M.Sc. (critical review and editing); Céline Dupuis, P. Geo., Ph.D. (English version); Nathalie Bouchard (HTML editing). 


Isabelle Lafrance, P. Geo., M.Sc. (redaction)

Mehdi A. Guemache, P. Geo., Ph.D. (coordination); Marc-Antoine Vanier, Eng., M.Sc. (critical review); Simon Auclair, P. Geo., M.Sc. (editing); Dominique Richard, GIT, Ph.D. (English version); André Tremblay (HTML editing). 

5 novembre 2018