Migmatite

Migmatite is a composite rock found in medium and high-grade metamorphic environments. It consists of two or more constituents often layered repetitively; one layer was formerly paleosome, a metamorphic rock that was reconstituted subsequently by partial melting; the alternate layer has a pegmatitic, aplitic, granitic or generally plutonic appearance. Commonly, migmatites occur below deformed metamorphic rocks that represent the base of eroded mountain chains, commonly within Precambrian cratonic blocks[1],

Ptygmatic folding in migmatite on Naissaar Island, Estonia

Migmatite on the coast of Saaremaa, Estonia

Intricately-folded migmatite from near Geirangerfjord, Norway

Migmatites form under extreme temperature and pressure conditions during prograde metamorphism, when partial melting occurs in metamorphic paleosome.[2] Components exsolved by partial melting are called neosome (meaning ‘new body’), which may or may not be heterogeneous at the microscopic to macroscopic scale. Migmatites often appear as tightly, incoherently folded veins (ptygmatic folds).[3] These form segregations of leucosome, light-colored granitic components exsolved within melanosome, a dark colored amphibole- and biotite-rich setting. If present, a mesosome, intermediate in color between a leucosome and melanosome, forms a more or less unmodified remnant of the metamorphic parent rock paleosome. The light-colored components often give the appearance of having been molten and mobilized.

The diagenesis - metamorphism sequence

An early geological cross-section of the Earth's crust.

Migmatite is the penultimate member of a sequence of lithology transformations first identified by Lyell, 1837.[4] Lyell had a clear perception of the regional diagenesis sequence in sedimentary rocks that remains valid today. It begins ‘’’A’’’ with deposition of unconsolidated sediment (protolith for future metamorphic rocks). As temperature and pressure increase with depth, a protolith passes through a diagenetic sequence from porous sedimentary rock through indurated rocks and phyllites ‘’’A2’’’ to metamorphic schists ‘’’C1’’’ in which the initial sedimentary components can still be discerned. Deeper still, the schists are reconstituted as gneiss ‘’’C2’’’ in which folia of residual minerals alternate with quartzo-feldspathic layers; partial melting continues as small batches of leucosome coalesce to form distinct layers in the neosome, and become recognizable migmatite ‘’’D1’’’. The resulting leucosome layers in stromatic migmatites still retain water and gas[5] in a discontinuous reaction series from the paleosome. This supercritical H₂O and CO₂ content renders the leucosome extremely mobile.

Bowen 1922, p184[6] described the process as being ‘In part due to … reactions between already crystallized mineral components of the rock and the remaining still-molten magma, and in part to reactions due to adjustments of equilibrium between the extreme end-stage, highly concentrated, "mother-liquor", which, by selective freezing, has been enriched with the more volatile gases usually termed "mineralizers," among which water figures prominently’. J.J. Sederholm (1926)[7] described rocks of this type, demonstrably of mixed origin, as migmatites. He described the granitising ‘ichors’ as having properties intermediate between an aqueous solution and a very much diluted magma, with much of it in the gaseous state.

Partial melting, anatexis and the role of water

The role of partial melting is demanded by experimental and field evidence. Rocks begin to partially melt when they reach a combination of sufficiently high temperatures (> 650°C) and pressures (>34MPa). Some rocks have compositions that produce more melt than others at a given temperature, a rock property called fertility. Some minerals in a sequence will make more melt than others; some do not melt until a higher temperature is reached[6]. If the temperature attained only just surpasses the solidus, the migmatite will contain a few small patches of melt scattered about in the most fertile rock. Holmquist 1916 called the process whereby metamorphic rocks are transformed into granulite ‘anatexis’.[8]

The segregation of melt during the prograde part of the metamorphic history (temperature > solidus) involves separating the melt fraction from the residuum, which higher specific gravity causes to accumulate at a lower level. The subsequent migration of anatectic melt flows down local pressure gradients with little or no crystallization. The network of channels through which the melt moved at this stage may be lost by compression of the melanosome, leaving isolated lenses of leucosome. The melt product gathers in an underlying channel where it becomes subject to differentiation. Conduction is the principal mechanism of heat transfer in the continental crust; where shallow layers have been exhumed or buried rapidly there is a corresponding inflection in the geothermal gradient. Cooling due to surface exposure is conducted very slowly to deeper rocks so the deeper crust is slow to heat up and slow to cool. Numerical models of crustal heating[9] confirm slow cooling in the deep crust. Therefore, once formed, anatectic melt can exist in the middle and lower crust for a very long period of time. It is squeezed laterally to form sills, laccolithic and lopolithic structures of mobile granulite at depths of c. 10–20 km. In outcrop today only stages of this process arrested during its initial rapid uplift are visible. Wherever the resulting fractionated granulite rises steeply in the crust, water exits from its supercriticality phase, the granulite starts to crystallize, becomes firstly fractionated melt + crystals, then solid rock, whilst still at the conditions of temperature and pressure existing beyond 8 km. Water, carbon dioxide, sulphur dioxide and other elements are exsolved under great pressure from the melt as it exits from supercritical conditions. These components rise rapidly towards the surface and contribute to formation of mineral deposits, volcanoes, mud volcanoes, geysers and hot springs.[10].

Color-banded migmatites

A leucosome is the lightest-colored part of migmatite.[11] The melanosome is the darker part, and occurs between two leucosomes or, if remnants of the more or less unmodified parent rock (mesosome) are still present, it is arranged in rims around these remnants.[11] When present, the mesosome is intermediate in color between leucosome and melanosome.[11]

Migmatite textures

Migmatite textures are the product of thermal softening of the metamorphic rocks. Schlieren textures are a particularly common example of granite formation in migmatites, and are often seen in restite xenoliths and around the margins of S-type granites.

Ptygmatic folds are formed by highly plastic ductile deformation of the gneissic banding, and thus have little or no relationship to a defined foliation, unlike most regular folds. Ptygmatic folds can occur restricted to compositional zones of the migmatite, for instance in fine-grained shale protoliths versus in coarse granoblastic sandy protolith.

When a rock undergoes partial melting some minerals will melt (neosome, i.e. newly formed), while others remain solid (paleosome, i.e. older formation). The neosome is composed of lightly-colored areas (leucosome) and dark areas (melanosome). The leucosome lies in the center of the layers and is mainly composed of quartz and feldspar. The melanosome is composed of cordierite, hornblende and biotite and forms the wall zones of the neosome.[2]

Early history of migmatite investigations

James Hutton (1795)[12] made some of the earliest comments on the relationship between gneiss and granite: “If granite be truly stratified, and those strata connected with the other strata of the earth, it can have no claim to originality; and the idea of primitive mountains, of late so much employed by natural philosophers, must vanish, in a more extensive view of the operations of the globe; but it is certain that granite, or a species of the same kind of stone, is thus found stratified. It is the granit feuilletée of M. de Saussure, and, if I mistake not, what is called gneis by the Germans.” The minute penetration of gneiss, schists and sedimentary deposits altered by contact-metamorphism, alternating with granitic materials along the planes of schistosity was described by Michel-Lévy 1887, in his paper ' Sur l'Origine des Terrains Cristallins Primitifs'[13] he makes the following observations: “I first drew attention to the phenomenon of intimate penetration, ‘lit par lit’ of eruptive granitic and granulitic rocks that follow the schistosity planes of gneisses and schists ... But in between, in the contact zones Immediately above eruptive rock, quartz and feldspars insert themselves, bed by bed, between the leaves of the micaceous shales; it started from a detrital shale, now we find it definitively transformed into a recent gneiss, very difficult to distinguish from ancient gneiss”. The coincidence of schistosity with bedding gave rise to the proposals of static or load metamorphism, advanced by Judd (1889),[14] Milch (1894),[15] and others. Vertical pressure due to the weight of the overlying load was recognized to be the controlling factor. Home and Greenly (1896) agreed that granitic intrusions are closely associated with metamorphic processes " the cause which brought about the introduction of the granite also resulted in these high and peculiar types of crystallization ".[16] A later paper of Edward Greenly (1903) described the formation of granitic gneisses by solid diffusion, and ascribed the mechanism of lit-par-lit occurrence to the same process. Greenly (1903) drew attention to thin and regular seams of injected material, which indicated that these operations took place in hot rocks; also to undisturbed septa of country rocks, which suggested that the expression of the magma occurred by quiet diffusion rather than by forcible injection.[17]. Sederholm (1907)[18] called the migmatite-forming process palingenesis. and (although it specifically included partial melting and dissolution) he considered magma injection and its associated veined and brecciated rocks as fundamental to the process. The upward succession of gneiss, schist and phyllite in the Central European Urgebirge influenced Grubenmann (1910, p. 138)[19] in his formulation of three depth-zones of metamorphism.

Comparison between anatexis and palingenesis interpretations of migmatite relationship with granulite

Holmquist [20] found high-grade gneisses that contained many small patches and veins of granitic material. Granites were absent nearby, so he interpreted the patches and veins to be collection sites for partial melt exuded from the mica-rich parts of the host gneiss. Holmquist gave these migmatites the name ‘venite’ to emphasize their internal origin and to distinguish them from Sederholm's ‘arterites’. Which also contained veins of injected material. Sederholm later placed more emphasis on the roles of assimilation and the actions of fluids in the formation of migmatites and used the term ‘ichor’, to describe them. Persuaded by the close connection between migmatization and granites in outcrop, Sederholm[21][22] considered migmatites to be an intermediary between igneous and metamorphic rocks. He thought that the granitic partings in banded gneisses originated through the agency of either melt or a nebulous fluid, the ichor, both derived from nearby granites. An opposing view, proposed by Holmquist, was that the granitic material came from the adjacent country rock, not the granites, and that it was segregated by fluid transport. Holmquist believed that such replacive migmatites were produced during metamorphism at a relatively low metamorphic grade, with partial melting only intervening at high grade. Thus, the modern view of migmatites corresponds closely to Holmquist's concept of ultrametamorphism, and to Sederholm's concept of anatexis, but is far from the concept of palingenesis, or the various metasomatic and subsolidus processes proposed during the granitization debate;

Cliff section through near-vertically dipping ptgmatically folded migmatites

(see Read 1952[23]). Read 1940, p. 249[24] considered that regionally metamorphosed rocks resulted from the passage of waves or fronts of metasomatizing solutions out from the central granitization core, above which arise the zones of metamorphism.

Agmatite

Intrusion breccia dyke at Goladoo, Co. Donegal, Ireland

The original name for this phenomenon was defined by Sederholm (1923)[25] as a rock with "fragments of older rock cemented by granite", and was regarded by him to be a type of migmatlte. There is a close connection between migmatites and the occurrence of ‘explosion breccias’ in schists and phyllites adjacent to diorite and granite intrusions. Rocks matching this description can also be found around igneous intrusive bodies in low-grade or unmetamorphosed country-rocks. Brown (1973) argued that agmatites are not migmatites, and should be called ‘intrusion breccias’ or ‘vent agglomerates’. Reynolds (1951)[26] thought the term ‘agmatite’ ought to be abandoned.

Migmatite melts provide buoyancy for sedimentary isostasy

Recent geochronological studies from granulite-facies metamorphic terranes (e.g. Willigers et al. 2001)[27] shows that metamorphic temperatures remained above the granite solidus for between 30 and 50 My. This suggests that once formed, anatectic melt can exist in the middle and lower crust for a very long period of time. The resulting granulite is free to move laterally[28] and up weaknesses in the overburden in directions determined by the pressure gradient.

In areas where it lies beneath a deepening sedimentary basin, a portion of granulite melt will tend to move laterally beneath the base of previously metamorphosed rocks that have not yet reached the migmatic stage of anatexis. It will congregate in areas where pressure is lower. The melt will lose its volatile content when it reaches a level where temperature and pressure is less than the supercritical water phase boundary. The melt will crystallise at that level and prevent following melt from reaching that level until persistent following magma pressure pushes the overburden upwards.

Other migmatite hypotheses

Migmatite at Maigetter Peak, Fosdick Mountains, West Antarctica

For migmatised argillaceous rocks, the partial or fractional melting would first produce a volatile and incompatible-element enriched rich partial melt of granitic composition. Such granites derived from sedimentary rock protoliths would be termed S-type granite, are typically potassic, sometimes containing leucite, and would be termed adamellite, granite and syenite. Volcanic equivalents would be rhyolite and rhyodacite.

Migmatised igneous or lower-crustal rocks which melt do so to form a similar granitic I-type granite melt, but with distinct geochemical signatures and typically plagioclase dominant mineralogy forming monzonite, tonalite and granodiorite compositions. Volcanic equivalents would be dacite and trachyte.

It is difficult to melt mafic metamorphic rocks except in the lower mantle, so it is rare to see migmatitic textures in such rocks. However, eclogite and granulite are roughly equivalent mafic rocks.

Etymology

The Finnish petrologist Jakob Sederholm first used the term in 1907 for rocks within the Scandinavian craton in southern Finland. The term was derived from the Greek word μιγμα: migma, meaning a mixture.

See also

• Anatexis
• List of rock textures – A list of rock textural and morphological terms
• Migmatitovaya Rock – A rock formation in Queen Maud land, Antarctica
• Rock microstructure – The texture of a rock and the small scale rock structures

References

1. Sawyer, Edward (2008). Atlas of Migmatites. The Canadian Mineralogist Special Publication 9. Mineralogical Association of Canada.
2. Mehnert, Karl Richard (1971). Migmatites and the origin of granitic rocks, Developments in Petrology. Elsevier.
3. Recommendations by the IUGS Subcommission on the Systematics of Metamorphic Rocks, Part 6. Migmatites and related rocks, p2.
4. Lyell, Charles (1837). Principles of Geology. London: John Murray.
5. Goransen, Roy (1938). "Silicate – Water Systems: Phase equilibria in the NaAlSi3O8 – H2O and KALSi3O8 – H2O Systems at High Temperatures and Pressures". American Journal of Science. 35A: 71–91.
6. Bowen, N (1922). "The Reaction Principle in Petrogenesis". Journal of Geology. 30 (3): 177–198. Bibcode:1922JG.....30..177B. doi:10.1086/622871.
7. Sederholm, J (1926). "On migmatites and associated rocks in Southern Finland II". Bull. Comm. Géol. Finlande. 77: 89.
8. Holmquist, P (1916). "Swedish Archean structures and their meaning". Bulletin of the Geological Institute Upsala. 15: 125–148.
9. England, Philip; Thompson, Bruce (1984). "Pressure—Temperature—Time Paths of Regional Metamorphism I. Heat Transfer during the Evolution of Regions of Thickened Continental Crust Journal of Petrology". Journal of Petrology. 25 (4): 894–928. doi:10.1093/petrology/25.4.894.
10. Lowenstern, Jacob (2001). "Carbon dioxide in magmas and implications for hydrothermal systems". Mineralium Deposita. 36 (6): 490–502. Bibcode:2001MinDe..36..490L. doi:10.1007/s001260100185.
11. Recommendations by the IUGS Subcommission on the Systematics of Metamorphic Rocks, Part 6. Migmatites and related rocks, p2.
12. Hutton, James (1798). Theory of the Earth {volume=1 }chapter=4. Edinburgh.
13. Michel-Lévy, A (1887). "Sur l'origine des terrains cristallins prirnitifs". Soc. Géol. France. 3 (14): 102.
14. Judd, John (1889). "On the Growth of Crystals in Igneous Rocks after their Consolidation". Quart. Journ. Geol. Soc. 45 (1–4): 175–186. doi:10.1144/GSL.JGS.1889.045.01-04.13.
15. Milch, L (1894). "Beitrage zur Lehre vonder Regionalmetamorphose". Neues Jahrb. F. Min. Geol. U. Pal. Beil.-Bd. 10: 101.
16. Horne, J (1896). "On foliated granites and their relations to the crystalline schists jn eastern Sutherland". Quart. Journ. Geol. Soc.: 633.
17. Greenly, Edward (1903). "The diffusion of granite into crystalline schists". Geol. Mag. 10 (5): 207. doi:10.1017/S0016756800112427.
18. Sederholm, J (1907). "Om granit och gneiss". Bull. De la Commission Géol. De Finlande. 4 (23).
19. Grubermann, U (1910). "Die kristallinen Schiefer". The Canadian Mineralogist Special Publication (Mineralogical Association of Canada).
20. Holmquist, p (1920). "Om pogrnatit-palingenes och ptygmatisk veckning". Geol. Fören. Stockholm Förh. 42 (4): 191. doi:10.1080/11035892009444463.
21. Sederholm, J (1907). "On Granite and gneiss: their origin, relations and occurrence in the Pre-Cambrium complex of Fennoscandia". Bull. Comm. Géol. Finlande: 207.
22. Sederholm, J (1926). "On migmatites and associated rocks in Southern Finland II". Bull. Comm. Géol. Finlande. 77: 89.
23. Read, H (1957). The Granite Controversy. Thomas Murby & Co.
24. Read, H (1940). ". Metamorphism and igneous action. Presidential Address to Section C, British Association, Dundee Meeting, 1939". Advancement of Science. 108: 223–250.
25. Sederholm, J (1923). "On migmatites and associated pre-Cambrian rocks of southwestern Finland, Part I. The Pellinge region". Bull. Comm. Géol. Finlande. 58: 153.
26. Reynolds, Doris (1951). "The geology of Slieve Gullion, Foughill and Carrickarnan". Transactions of the Royal Society of Edinburgh. 62: 62–145.
27. Willigers, B; Krogstad, E; Wijbrans, J (2001). "Comparison of thermochronometers in a slowly cooled granulite terrain: Nagssugtoqidian Orogen, West Greenland". Journal of Petrology. 42 (9): 1729–1749. Bibcode:2001JPet...42.1729W. doi:10.1093/petrology/42.9.1729.
28. Bronguleev, V; Pshenin, G (1980). "Structure Forming Role of Isostatic Movements". In Nils-Axel Mörner (ed.). Earth Rheology, Isostasy and Eustasy. New York: John Wiley & Sons.