December 2017 Issue Table of Contents
Last year (2016), when I spoke at the Geological Society of America’s Penrose Conference on “Layered Mafic Intrusions and Associated Economic Deposits” held in Red Lodge, Montana, I noted that I gave my first professional talk some 35 years ago. As a young researcher back then, I had thought that all the interesting questions in layered intrusions were soon to be solved, leaving little room for me to make a name for myself. I was wrong!
Layered intrusions are important for a number of reasons. Primarily, they present a record of how mafic magmas crystallize and, as a consequence, change their compositions by the process of magmatic differentiation. However, it is increasingly recognized that deciphering the record preserved by layered intrusions is not as easy as once thought. The classic models envisioned that magma differentiation was the result of crystals settling out of the magma. Alternatively, it has been suggested that crystals precipitate ‘in situ’ on the floor and the walls of the magma chamber and that it is the evolved liquid that moves away from the crystals. Yet others have suggested that it is descending plumes of crystal-rich magma that accumulate at the floor of the magma chamber and then separate solid from liquid by compaction of the crystal pile. Layered intrusions also host important ore reserves of Ni, Cu, Cr, Ti, V, and unrivalled platinum-group element deposits; however, the mechanisms by which these elements have been concentrated are still hotly debated. Finally, the larger layered intrusions with sill-like geometries (e.g. the Bushveld Complex of South Africa) that intruded into previously unheated sediments can have basal metamorphic aureoles several kilometers thick. The geometry of dehydrating country rock overlain by hot ultramafic rock is similar to that occurring in subduction zones, and, hence, these large ultramafic/mafic sill systems are potentially excellent analogs for understanding fluid migration from descending slabs into the overlying mantle wedge. If correct, layered intrusions will allow us to better understand how fluids, which come off a dehydrating ocean crust slab, can maintain their isotopic signatures and induce melting by lowering the melting temperatures as they move into the mantle.
My views on layered intrusions have been influenced by the study of the larger examples, such as the Bushveld Complex and the Stillwater Complex (Montana, USA). These intrusions had a long time to be modified as they slowly cooled and crystallized. I have taken as my initial hypothesis that magmas simply crystallize and fractionate along a cotectic, and that many of the more interesting features of layered intrusions, including in many cases the layering itself, are imparted later. The thick sections of rather homogeneous igneous rock that occur in intrusions from the Skaergaard Intrusion of Greenland to the Stillwater Complex are, perhaps, the purest expression of how unexciting most of the crystallization of these magmas can be. Interest begins to peak once heterogeneities appear, whether it be the trough bands developed in the Skaergaard gabbro or the reappearance of olivine in the Banded Series of the Stillwater Complex. In my view, the central problem posed by layered intrusions is the extent to which they faithfully record magmatic processes and to what extent the magmatic textures and compositions have been modified by subsequent processes.
The conventional view is that layered intrusions are largely “constructive”, i.e. the rocks record the progressive crystallization of one or more magmas or their mixtures. That is, much of the character of the rock is directly the result of magma crystallization, with rock composition and grain size being a function of crystal nucleation and growth kinetics as well as variations of trapped liquid within the porous crystal pile. Rock texture and liquid proportions may be modified by compaction, but, in general, the bulk rock is considered a mixture of one or more minerals that have crystallized along a cotectic, plus some proportion of trapped liquid. The reintroduction of more primitive (i.e. Mg-rich, Si-poor) magma, or magmas with a different crystallization sequence, or crystal-bearing magmas, all represent potential complications associated with open system behavior but still lead to constructive growth of the crystal pile.
A more unconventional view, held by scientists such as myself, is the rocks undergo extensive modification over the many thousands to tens of thousands of years that it takes the rocks to solidify. For example, my work in the Stillwater Complex has convinced me that the platinum-rich J-M Reef was due to alteration and remelting of the original magmatic assemblage driven by the introduction of later mineralizing fluids. The mechanisms that drive these changes are, in a broad sense, “destructive” in that they modify or destroy the originally precipitated mineral assemblage. These “destructive” mechanisms can be as modest as simple crystal aging, by which large gains can grow at the expense of smaller grains (Ostwald ripening). Although a common process, modeling has suggested that crystal aging in a thermal or compositional gradient can produce size-graded layers, doublets, sharp modal boundaries, and other sedimentary-like features that need not have been present when the rock first started to crystallize (Fig. 1A). To paraphrase a statement made by Allen Glazner (Professor of Geological Sciences at the University of North Carolina, USA) at the 2016 Penrose Conference, “Using the rocks as they now appear to infer magmatic processes is about as difficult as trying to decipher sedimentary process from a metamorphic rock.”
Another process, which I believe can modify the original magmatic crystalline assemblage is compositional zone-refining whereby liquids and vapor migrate through the crystal mush. This may lead, in some instances, to wholesale remelting or replacement of the original mineral assemblage (McBirney 1987). This is most evident when the process results in bodies that crosscut layering. For example, the Middle Banded Series of the Stillwater Complex contains troctolites (rocks composed of olivine and plagioclase) that crosscut gabbros (composed of pyroxene and plagioclase) (Fig. 1B). Not only is there a change in the mineralogy, but there is a textural change from a well-foliated mineral lamination in the gabbro—in which the tabular minerals are all lying in the same plane—to a massive texture of unaligned minerals in the troctolite. These relationships have been explained by the interaction of the gabbroic protolith with fluids that became silica-undersaturated as they rose through the crystal pile, i.e. rose into hotter rocks. What this implies is that a reactive agent (a melt or fluid) can migrate through the crystal pile at high temperature and leave little evidence of its passage until it becomes out of equilibrium with the host assemblage.
The problems described above become even more acute when the modification of an original magmatic assemblage and texture is more or less conformable with the original layering, and it becomes difficult to infer what was a primary feature of the crystallizing magma and what occurred at a later stage. An example of this is the transition between poikilitic (a texture describing an igneous rock in which large crystals contain inclusions of other minerals) and an equigranular (a texture in which euhedral crystals are of equal size) harzburgite in a typical cyclic unit from the Ultramafic Series of the Stillwater Complex that can develop “finger structures” in which the poikilitic harzburgite forms thin pipe-like intrusions into the overlying granular harzburgite (Fig. 1C). This geometry is typical of structures that develop at reaction fronts (e.g. Kelemen et al. 1995; Boudreau 2016). Regardless of the actual cause, the finger structures and the possibility of one rock having formed by replacement of another suggests that the poikilitic harzburgite may not have initially crystallized as conventionally thought.
My work has convinced me that the use of “cumulus” terminology is one of the major impediments to understanding layered intrusions. This is because the terms, derived from the idea that the rock formed by “accumulated” minerals, has genetic/interpretive implications. Yet, these terms have been used for decades to describe the rocks. Although in many instances it may be true that some of the layered rocks formed as conventional cumulates, the examples noted above suggest this is not always the case. For example, the ultramafic rocks from the Stillwater can be texturally similar to mantle peridotites, but no one uses cumulus terminology to describe the latter. Other examples are those rocks interpreted to have formed by incongruent hydration melting—rocks more properly interpreted as “restites” (residual solid assemblages), not cumulates (e.g. Boudreau 1988, 1999)—and those rocks subject to metasomatic changes (e.g. Irvine 1980).Using a neutral descriptive terminology allows one to be open to other interpretations. It may be that nine times out of ten a conventional interpretation is correct, but why be prejudicial in the observational description of the rocks?
All of this, somewhat ironically, has led me to see that studies of large intrusions may not be the best way to understand how magmas crystallize. There is just too much overprinting and modification of the original mineralogy and texture. One of the avenues I find particularly promising is the integration of observations from small to large basaltic magma systems. For example, thick lava flows can show significant textural, lithological, and geochemical features that developed as the result of compaction (e.g. Philpotts et al. 1996). At the other extreme is the integration of observations from high-grade metamorphic rocks. For example, metamorphic banding can have many similarities with fine-scale mineral layering in layered intrusions, and both the igneous and metamorphic systems can show extensive evidence for isotopic disequilibrium. In regard to the latter, it is observed that grain-scale interaction of fluids based on isotope reequilibration is on the order of 103–105 years for amphibolite–granulite facies metamorphic rocks (e.g. Graham et al. 1998). The longer times are approximately the timescales of crystallization of the larger intrusions, and exploration of similarities with high-grade metamorphic isotopic disequilibrium may yet bring insights into the igneous problem.
This brings me back to my original concern as a young geologist: “No more interesting questions to be explored in layered intrusions?” Nah! We are just getting started…
Boudreau AE (1988) Investigations of the Stillwater Complex. IV. The role of volatiles in the petrogenesis of the J-M Reef, Minneapolis adit section. Canadian Mineralogist 26: 193-208
Boudreau AE (1999) Fluid fluxing of cumulates: the J-M reef and associated rocks of the Stillwater Complex, Montana. Journal of Petrology 40: 755-772
Boudreau AE (2016) The Stillwater Complex, Montana - Overview and the significance of volatiles. Mineralogical Magazine 80: 585-637
Graham CM, Valley JW, Eiler JM, Wada H (1998) Timescales and mechanisms of fluid infiltration in a marble: an ion microprobe study. Contributions to Mineralogy and Petrology 132: 371-389
Irvine TN (1980) Magmatic infiltration metasomatism, double diffusive fractional crystallization, and adcumulus growth in the Muskox intrusion and other layered intrusions. In: Hargraves RB (ed) Physics of Magmatic Processes. Princeton University Press, Princeton, NJ, pp 325-383
Kelemen PB, Whitehead JA, Aharonov E, Jordahl KA (1995) Experiments on flow focusing in soluble porous media, with applications to melt extraction from the mantle. Journal of Geophysical Research: Solid Earth 100: 475-496
McBirney AR (1987) Constitutional zone refining of layered intrusions. In: Parsons I (ed) Origins of Igneous Layering. D. Reidel, Boston, pp 437-452
Philpotts AR, Carrol M, Hill JM (1996) Crystal-mush compaction and the origin of pegmatitic segregation sheets in a thick flood-basalt flow in the Mesozoic Hartford Basin, Connecticut. Journal of Petrology 37: 811-836