Scott A. Whattam- Department of Geosciences, King Fahd University of Petroleum and Minerals, Dhahran, Saudi Arabia
Primitive magmatic rocks with Mg# ≥60 have been identified in the literature from the Sona-Azuero, Golfito and Chagres-Bayano forearc segments of southern Costa Rica and Panama of the early (75–39 Ma) Central American Volcanic Arc system (CAVAS). Primitive CAVAS basalts are remarkably similar in terms of major and many trace elements to primitive MORB and primitive basalts of the Mariana Arc and share affinities with global intra-oceanic arc tholeiitic and calc-alkaline basalts. Significant differences however, are apparent between primitive lavas of Chagres-Bayano relative to those of Sona-Azuero and Golfito. Primitive Chagres-Bayano lavas record much higher degrees of partial melting and higher amounts of shallow and deep subduction additions (e.g., higher Ba/Th, Th/Nb) than those of the older Sona-Azuero and Golfito arc segments which reflects the early petrologic and tectonic evolution of the CAVAS which is similar to other forearc systems. As shown in previous studies, early CAVAS lavas are exceptionally similar in radiogenic isotopic composition to those of the Caribbean Large Igneous Province (CLIP) oceanic plateau at 90 Ma, the approximate timing of onset of the volumetrically dominant phase of CLIP magmatism. Moreover, calculated potential temperatures of 1,633 ± 47°C for two Sona-Azuero primitive basalts suggests an anomalously hot mantle source at subduction initiation (SI). These insights are consistent with SI models which require a plume-induced SI scenario and an elevated sub-arc thermal anomaly upon inception of the CAVAS. It is postulated that, in addition to providing an anomalously high temperature regime in the sub-arc mantle at inception of the CAVAS, extrusion of the CLIP also resulted in lithospheric weakening and extension which allowed for production and rapid ascent of a high percentage of primitive magmas.
Introduction
Subduction zone magmatism (see review of Pearce and Peate, 1995) results primarily due to slab dehydration and the subsequent transfer of fluids from the dehydrating and metasomatically altered oceanic slab and its sediment cover to the mantle wedge where partial melting occurs (Tatsumi et al., 1983; White and Patchett, 1984; McCulloch and Gamble, 1991; Hawkesworth et al., 1993a,b; Plank and Langmuir, 1993; Ishikawa and Tera, 1999). Magmatic intra-oceanic arc systems (see review of Stern, 2010 and references therein) such as that of which the Central American Volcanic Arc system (CAVAS) was at subduction initiation (SI) represent the surface manifestation of large-scale, upper mantle melt extraction events at intra-oceanic subduction zones. The diagnostic chemical signature of subduction zone magmas is enrichment of large ion lithophile elements (LILE) relative to the light rare earth elements (LREE) and high field strength elements (HFSE) (e.g., Arculus, 1994). This signature is a function of a variety of parameters, for example, the mode and extent of partial melting, composition and thermal state of the mantle, and the relative contributions of fluids and sediments to the source. Intra-oceanic arcs represent the most important site of juvenile (mantle-derived) continental crust formation and are considered as fundamental building blocks of continents. Estimates of the mass proportion of continents formed at subduction zones are of the order of ~85–95% (Rudnick, 1995; Barth et al., 2000).
Most arc magmas are fractionated and relatively evolved with ~4–6 wt. % MgO (e.g., Tamura and Tatsumi, 2002; Kelemen et al., 2003; Tamura, 2003) and Mg#'s (Mg/Mg+Fe) that are too low to have equilibrated with mantle peridotite. In contrast, high-MgO (MgO > 8 wt. %) or primary (with Mg # of ~ ≥70 and high Ni > 200 ppm and Cr > 400 ppm) magmas (Tatsumi and Eggins, 1995) representing mantle partial melts minimally affected by fractionation, assimilation, mixing and storage are relatively uncommon in modern subduction zone settings. Nonetheless, primary or near-primary lavas (“primitive“ lavas least affected by fractional crystallization and assimilation) have been recovered from many intra-oceanic arc systems including the Izu-Bonin Marianas (Tamura et al., 2011, 2013), Solomon Islands (Schuth et al., 2004), Vanuatu (Eggins, 1993), Papua-New Guinea (Smith et al., 1997; Smith, 2013), the Aleutians (Kelemen et al., 2003), Lesser Antilles (Macdonald et al., 2000; Melekhova et al., 2015) the South Sandwich Islands (Leat et al., 2003) and Kamchatka (Hochstaedter et al., 1996; Portnyagin et al., 2007) but are usually volumetrically minor. Primary magmas have unfractionated compositions in equilibrium with upper mantle peridotite (Sato, 1977) and are of great petrological significance and constitute valuable sources of information on the conditions of partial melting and the thermal structure of the mantle wedge beneath volcanic arcs. Information on the conditions of petrogenesis of high-MgO arc basalts has come mainly from experimental studies. Many high-pressure experimental studies on high-MgO arc basalts have been performed under anhydrous (Tatsumi, 1982; Tatsumi et al., 1983, 1994; Gust and Perfit, 1987; Kushiro, 1987; Bartels et al., 1991; Draper and Johnson, 1992; Baker et al., 1994) and hydrous (Tatsumi, 1982; Tatsumi et al., 1983; Baker et al., 1994) conditions. Unfortunately, characteristic experimental f O2 conditions have generally been too reducing for arc settings (Tatsumi, 1982; Tatsumi et al., 1983; Gust and Perfit, 1987; Bartels et al., 1991; Draper and Johnson, 1992) rendering only a very limited number of experimental studies to be applicable to real conditions of basaltic melt generation in subduction zones. A recent study (Schmidt and Jagoutz, 2017) has provided valuable insights into the petrogenesis of global primitive arc melts (see Discussion).
The rarity of primary magmas in arc sequences has been attributed by Smith et al. (1997) to their high density and the relatively buoyant nature of the arc crust, which acts as a barrier to the ascent of dense, Mg-rich magmas and by Leat et al. (2002) to the difficulty in traversing the crust without encountering magma chambers. In a study of phase relationships of magnesian arc magmas, Pichavant and Macdonald (2003) argue that only the most water-poor primitive magmas are able to traverse the crust without adiabatically freezing, explaining the rarity of primitive magmas in arcs. This raises further questions about the extent to which erupted and sampled primary magmas in arcs are typical of mantle-derived melts in arcs. There is a related debate about the origin of high-Al basalts, which have greater than c. 17 wt. % A12O3 and are characteristic of arcs. Crawford et al. (1987) reviewed the arguments and concluded that accumulation of plagioclase was the origin of the high Al abundances. These debates highlight the difficulty in modeling fractionation histories of arc magmas, even in intra-oceanic arcs, where primitive magmas are usually absent, and both addition and fractional removal of phenocrysts has occurred.
If mantle-derived magmas are Mg-rich, the transition from primitive melts to low-Mg basalts by fractional crystallization must generate significant thicknesses of mafic and ultramafic cumulates. This is consistent with the presence of high-velocity (P-wave velocity = 6.9–7.5 km s−1) layers several kilometers thick that have been seismically detected at the base of the crust in some intra-oceanic arcs (Suyehiro et al., 1996; Holbrook et al., 1999). Similarly, seismic velocity measurements on samples of exposed lower crust of the exhumed Kohistan Arc (Pakistan) for example, strongly suggest that these high-velocity keels consist of ultramafic cumulates (Miller and Christensen, 1994).
A number of studies have considered the older or early (Late Cretaceous to Eocene) segments of the CAVAS (e.g., Lissinna, 2005; Buchs et al., 2010; Wegner et al., 2011; Montes et al., 2012; Whattam and Stern, 2015). However, none of these studies have considered explicitly the existence of “primitive” lavas in the early (75–39 Ma) CAVAS in southernmost Costa Rica and Panama. I use the terms “primitive” and “evolved” lavas to encompass those with ≥ 60 and < 60 Mg#, respectively. Subsequently, I explain the basic petrogenesis of these high-Mg primitive lavas, compare these with other primitive arc suites and discuss its significance in the context of the chemical and tectonic evolution of the CAVAS.
Geological Background and Regional Setting
Presently, the Quaternary to modern-day CAVAS volcanic front stretches ~1,100 km along the western margin of the Caribbean plate from Costa Rica through Nicaragua, El Salvador and Guatemala to the Guatemala-Mexico border at the southern margin of the North American plate (Figure 1A). However, upon inception of unequivocal arc-related magmatism at the CAVAS by ~75 Ma (Buchs et al., 2010), the volcanic arc system bordered the entirety of southernmost present-day Panama (Lissinna, 2005; Wörner et al., 2009; Buchs et al., 2010; Wegner et al., 2011) and appears to have swept as far east as present-day western Colombia (Lissinna, 2005; Montes et al., 2012; Whattam and Stern, 2015) and possibly as far west as the Nicoya peninsula in present-day northwestern Costa Rica (Whattam and Stern, 2015). Inception of subduction at the CAVAS has been posited as the result of plume-induced (Whattam and Stern, 2015) or collision-induced (e.g., Buchs et al., 2010) SI following extrusion of the Caribbean Large Igneous Province (CLIP). Subsequent to northeasterly migration of the CLIP and “sandwiching” of the CLIP between the North and South American continents, the CAVAS was constructed upon the CLIP (e.g., as in Buchs et al., 2010; see also model of Hoernle et al., 2002, which is based on models referenced therein).
Figure 1. Maps of (A) the greater Caribbean region showing the distribution of the Caribbean Plate and the modern (2.6–0 Ma) Central American Volcanic Arc system (CAVAS, black triangles) and (B) the location and distribution of the three early (75–39 Ma) CAVAS segments at Sona-Azuero, Golfito and Chagres-Bayano investigated in this study.
After the Eocene, the foci of CAVAS magmatic activity shifted from east to west. Older exposures generated to the east comprise the 75–39 Ma Sona-Azuero, 75–66 Ma Golfito and 70–39 Ma Chagres-Bayano complexes in southernmost Costa Rica and Panama (Figure 1B). The Sona-Azuero and Chagres-Bayano complexes are interpreted as being floored by segments of the 89–85 Ma CLIP (Wörner et al., 2009; Buchs et al., 2010; Wegner et al., 2011; Montes et al., 2012). The Golfito Complex has been interpreted as both CLIP oceanic plateau (Hauff et al., 2000a) and more recently as arc (Buchs et al., 2010). Prior to the study of Buchs et al. (2010), it has generally been assumed that most oceanic forearc units along western Costa Rica and Panama represented uplifted segments of the CLIP (e.g., Hauff et al., 2000a). Similar interpretations have been made for many oceanic complexes along NW South America and the Leeward Antilles (see Whattam and Stern, 2015).
Relatedly, most researchers have posited two separate tectonic environments of formation to explain the oceanic plateau-arc association—an initial one for the CLIP at a within-plate setting—and a subsequent, younger one for the arc segments above a subduction zone to the rear of the CLIP. According to this model, CAVAS construction in Panama and southernmost Costa Rica began at ~ 75 Ma (e.g., Buchs et al., 2010) atop the pre-existing CLIP oceanic plateau subsequent to Farallon Plate (now the Cocos Plate) subduction beneath the CLIP plateau (e.g., Hauff et al., 2000a and references therein). Alternatively, Whattam and Stern (2015) consider both units as “plume- and arc-related” ones that represent hybrid units which formed simultaneously to or soon after plateau extrusion in a single, rapidly evolving tectonic environment.
Many CAVAS studies have focused on the geochemical and isotopic evolution of the Quaternary to modern-day volcanic front (e.g., see references in CentAm and IBM Geochem Database version 1.02 at: http://www.earthchem.org/grl). Two recent papers (Gazel et al., 2015; Whattam and Stern, 2016) have provided synergistic chemotemporal treatments of the CAVAS from inception at ~75 Ma to the present day in Costa Rica and Nicaragua. In each of these studies (Gazel et al., 2015; Whattam and Stern, 2016) it was concluded that the production of arc magmas with continental crust compositions was achieved in the CAVAS by about 15 Ma. It was further demonstrated by Whattam and Stern (2016) that the CAVAS records a gradual enrichment in incompatible element concentrations with time which they attributed to gradual thickening of the arc substrate and depression of mantle geotherms and a concomitant decrease in the degree of partial melting. For a more in-depth treatment of the chemical aspects and evolution of the CAVAS, I refer readers to the aforementioned studies.
Samples and Methods
Primitive lavas (those with ≥ 60 Mg#) in the literature from three early (75–39 Ma) CAVAS forearc segments at Sona-Azuero (Buchs et al., 2010; Wegner et al., 2011; Whattam et al., under review) and Chagres-Bayano (Wegner et al., 2011; Montes et al., 2012) in southwestern and eastern Panama, respectively, and Golfito (Buchs et al., 2010) of southernmost Costa Rica (Figure 1, Table 1) are recognized. The number of primitive lava samples identified from Sona-Azuero, Chagres-Bayano and Golfito is 6, 17 and 3 respectively, which comprise 11, 19, and 38% of the total (that is, primitive plus non-primitive, or evolved) samples of each complex (Figure 2). For comparison with early CAVAS primitive magmas, I also use compositions of primitive MORB (Jenner and O'Neill, 2012), primitive lavas of segments of two western Pacific arc systems at Papua, New Guinea (Smith et al., 1997; Smith, 2013) and the Izu-Bonin Mariana Arc system (Tamura et al., 2011) and global intra-oceanic arcs (Schmidt and Jagoutz, 2017).
Table 1. Whole rock major and trace element compositions of primitive CAVAS lavas from the Sona-Azuero, Golfito, and Chargres-Bayano arc segments.
Figure 2. Histograms of Mg# of Sona-Azuero, Golfito, and Chagres-Bayano lavas to demonstrate the number of lavas of each suite which have low Mg#, moderately high Mg# and high Mg#.
Samples were filtered to include only volcanic rocks with loss on ignition (LOI) <3 wt. % which yield anhydrous oxide totals of 96–101 wt. %. In the case of the datasets of Wegner et al. (2011), which do not provide LOI, only the 96–101 wt. % filter is applied. In the study of Buchs et al. (2010) major elements were analyzed via an X-Ray fluorescence (XRF) spectrometer and trace element concentrations were obtained on a laser ablation inductively coupled plasma mass spectrometer (LA-ICP-MS). In the study of Wegner et al. (2011), concentrations of major and minor elements (Si, Ti, Al, Fe, Mn, Mg, Ca, Na, K, and P) as well as selected trace elements (Nb, Zr, Y, Sr, Rb, Ga, Zn, Cu, Ni, Co, Cr, V, Ba, and Sc) were analyzed by XRF whereas the REE, high-field strength elements (HFSE: Nb, Ta, Zr, and Hf), large-ion lithophile elements (LILE: Rb, Sr, Ba, and Cs) and a group of other trace elements (Li, Sc, Cu, V, Cr, Co, Ni, Zn, Y, Pb, Th, and U) were analyzed via ICP-MS. In the study of Montes et al. (2012), major elements were determined by XRF and trace elements via LA-ICP-MS whereas the in the study of Whattam et al. (under review), major and trace elements were determined by ICP-atomic emission spectrometry (ICP-AES).
Results
Etrography, Alteration, and Low-T Metamorphism
As this is a study of data in the literature, most samples discussed are not available for petrographic description. Nonetheless, according to the literature from which these samples are recognized (Buchs et al., 2010; Wegner et al., 2011; Montes et al., 2012) including Whattam et al. (under review), the Sona-Azuero and Golfito lavas consist essentially of clinopyroxene, plagioclase and groundmass; olivine is not present. For example, in the aforementioned papers there is no mention of olivine apart from it comprising the non-arc related plateau and enriched Type II basalts (Buchs et al., 2010; Whattam et al., under review). According to Whattam et al. (under review), Azuero evolved lavas usually display micro-porphyritic and sometimes robustly porphyritic textures defined by large (1.5–2.0 mm), commonly euhedral, fresh clinopyroxene phenocrysts. The crystallization sequence is clinopyroxene followed by plagioclase which is typical of hydrous (i.e., arc) magmas in which early plagioclase crystallization is suppressed (Pearce et al., 1984; Cameron, 1985; Sisson and Grove, 1993).
Though the studies of Buchs et al. (2010), Wegner et al. (2011), Montes et al. (2012) and Whattam et al. (under review) concede some alteration, the samples considered were chosen on the basis of freshness and only samples with oxide totals of 96–102 wt. % and LOI <3.0 wt. % are considered in this study. To demonstrate the apparent freshness of the primitive samples of this study, I plot all primitive and evolved lavas of Sona-Azuero, Golfito and Chagres-Bayano in total alkalis vs. SiO2 (TAS) (Figure 3A) and Zr/Ti vs. Nb/Y (Figure 3B) space. I use these plots not for classification purposes but rather for comparative ones in order to look at possible alteration. For example, SiO2, K2O, and Na2O are known to be mobile whereas Zr, Ti, Nb, and Y are not. Thus, by comparing Figure 3A with Figure 3B I can comment on the apparent alteration undergone by these CAVAS forearc lavas. A comparison of Figures 3A,B demonstrates that a moderate number of evolved samples have elevated total alkalis which results in their plotting within the alkaline lavas fields in Figure 3A, which is likely the result of mobilization of these elements and alteration as these same samples do not plot as alkaline in Figure 3B. I note that none of the primitive samples appear to have been subjected to the addition of alkalis.
Figure 3. (A) Total alkalis-silica (TAS) (Le Bas et al., 1986) and (B) Zr/Ti vs. Nb/Y (Winchester and Floyd, 1977) plots of primitive and evolved lavas of Sona-Azuero, Golfito and Chagres-Bayano. Note that one evolved Chagres-Bayano basalt plots of the diagram to the left with ~0.006 Nb/Y and 0.007 Zr/Ti. Abbreviations: PA, A and A beside symbols here and in subsequent figures: proto-arc, arc (squares, circles).
Furthermore, a plot of LOI vs. various potentially mobile elements (MgO, K2O, CaO, Na2O, and Ba, Supplementary Figure 1) show no correlation suggesting that these CAVAS have not been significantly affected by alteration. Finally, my geochemical plots and arguments rely primarily on trace elements known to be immobile up to greenschist-facies metamorphic conditions.
Olivine Accumulation
As the lavas considered in this study comprise nil reported olivine, the high MgO contents (up to 10.41 wt. % MgO) are likely not the result of olivine accumulation. Plots of FeOt vs. MgO (Supplementary Figure 2A) support that no olivine accumulation (i.e., a trend of decreasing MgO with decreasing FeOt) occurred, whereas high correlation between Cr and Ni with R2 values of 0.83–0.96 (Supplementary Figure 2B) supports this conclusion.
Relation Between Primitivity and Age
Although ages (Wegner et al., 2011) are available for only some of the samples considered in this study (Table 2) the available ages demonstrate that the three oldest ones have Mg# >60 and that primitive lava production was restricted to the interval between subduction inception and ~66 Ma. This suggests that at least some of the oldest samples which have been generated soon after subduction inception are primitive and that assuming a relation between plume emplacement and generation of early primitive lavas may be valid. Moreover, five primitive samples are proto-arc basalts and these basalts are assumed to have formed early in the evolution of the CAVAS circa 75–66 Ma (Buchs et al., 2010).
Table 2. Relation between age and primitivity.
MgO, Ni, and Cr Contents
Primary magmas are ones in equilibrium with mantle peridotite and hence have high MgO and compatible element (Ni, Cr) concentrations. A line of MgO = 30 – (0.43 × SiO2) was empirically derived by Smith and Mitchell (1989) to delineate a suite of high-Mg lavas of the Papuan volcanic arc which plot above the line in SiO2 vs. MgO space from low-Mg lavas which plot below the line. In Figure 4 I plot MgO vs. SiO2 of all early CAVAS lavas with the line of MgO = 30 – (0.43 × SiO2) superimposed upon it. This line demarcates primitive from non-primitive CAVAS lavas relatively well but with some exceptions. For example, 15% (11 of 74) of non-primitive (evolved) lavas with Mg# < 60 plot above the line of MgO = 30 – (0.43 × SiO2) whereas 29% (6 of 21) of primitive lavas with Mg# ≥ 60 plot below this line. Also superimposed on Figure 4 are two dotted lines at SiO2 = 52 wt. % and MgO = 8 wt. % to demonstrate that the majority of primitive basalts (67%) have > 8 wt. % MgO whereas only 7% of the evolved basalts have > 8 wt. % MgO.
Figure 4. SiO2 vs. MgO of evolved lavas (Mg# < 60, top) and primitive lavas (Mg# >60, bottom) of Sona-Azuero, Golfito and Chagres-Bayano. The black line in each plot represents the equation MgO = 30-(0.43*SiO2) (Smith and Mitchell, 1989) (see text) which subdivides primitive Papuan Arc lavas which plot above the line from normal or evolved Papuan Arc lavas. The numbers in italics represent Mg# of the adjacent symbols.
A plot of Cr vs. Ni (Supplementary Figure 2B) demonstrates that the vast majority (70%) of the primitive lavas have either >100 ppm Ni or >150 ppm Cr or both. The Chagres-Bayano primitive lavas are the most Ni and Cr rich and reach Ni and Cr contents of 323 ppm and 714 ppm, respectively. In contrast, most evolved lavas have <50 ppm Ni and <100 ppm Cr. The CAVAS primitive lavas are similar in terms of Ni and Cr contents with primitive MORB and primitive lavas of the Mariana and Papuan arcs but three Chagres-Bayano primitive samples extend to both higher Ni and Cr concentrations than all three of these suites.
Chondrite Normalized REE and N-MORB Normalized Patterns
Chondrite normalized REE patterns of early CAVAS basalts are shown in Figure 5. Primitive lavas of the Sona-Azuero and Golfito suites comprise a relatively low percentage of the total samples (9 and 18% respectively, Figure 2) and in each suite, the ∑REE of the primitive basalts are lower than that of the evolved basalts. In the case of the Sona-Azuero suite, the ∑REE of the primitive basalts range from 54 to 60 and exhibit REE concentrations of ~15× chondrite whereas the evolved basalts exhibit a ∑REE range of 31–208. Chondrite normalized La/Yb ([La/Yb]CN) also rises to much higher values in the evolved Sona-Azuero basalts relative to the primitive Sona-Azuero basalts. REE patterns of the primitive Sona-Azuero basalts are flat to slightly LREE-enriched ([La/Yb]CN = 1.13–1.24) whereas the REE patterns of the evolved basalts range to moderately fractionated patterns ([La/Yb]CN = 0.75–3.45). Similarly, the primitive Golfito basalts exhibit lower ∑REE (21–27) than their evolved counterparts (∑REE of 49–59). [La/Yb]CN of the primitive Golfito basalts are 0.64–0.83 whereas the evolved Golfito basalts exhibit [La/Yb]CN of 0.61–0.88. In contrast, primitive lavas occupy a high percentage of the Chagres-Bayano suite (37%) and the primitive basalts overlap the evolved basalts in terms of both ∑REE and [La/Yb]CN. Primitive Chagres-Bayano basalts have ∑REE of 19–96 and [La/Yb]CN of 0.58–1.51 whereas the evolved Chagres-Bayano basalts have ∑REE of 39–87 and [La/Yb]CN of 0.43–3.28. That the primitive Chagres-Bayano basalts range to the lowest ∑REE and [La/Yb]CN suggests that they were derived from a more depleted source and/or higher degrees of partial melting than the Sona-Azuero and Golfito lavas. In all three suites, the HREE from Ho to Lu have gentle slopes or are nearly flat which demonstrates the general absence of residual garnet in the source of all three suites, a feature of which is characteristic of global arc suites (Schmidt and Jagoutz, 2017).
Figure 5. Chondrite normalized REE concentrations of primitive basalts of (A) Sona-Azuero, (B) Golfito, and (C) Chagres-Bayano vs. evolved basalts of each arc segment. Chondrite abundances from Sun and McDonough (1989).
N-MORB normalized patterns of the primitive early CAVAS lavas are shown in Figure 6. All three arc segments exhibit the classical features of arc magmatism, that is, LILE enrichment and HFSE depletion. Superimposed on the background of Figure 6 are the N-MORB normalized patterns of the evolved lavas of each suite which highlights differences between the primitive and evolved lavas although the patterns are broadly similar. In terms of LILE enrichment among the primitive suites, the Sona-Azuero and Golfito arc segments are mildly enriched (e.g., N-MORB normalized Ba ([Ba]NMM) of 11–16) whereas the Chagres-Bayano arc segment ranges to strongly LILE enriched ([Ba]NMM] of up to 148).
Figure 6. N-MORB normalized concentrations of primitive basalts of (A) Sona-Azuero, (B) Golfito, and (C) Chagres-Bayano vs. evolved basalts of each arc segment. N-MORB abundances from Sun and McDonough (1989).
Discussion
Silica Variation Diagrams
On Figure 7, I plot SiO2 vs. major element oxides (Figure 7A), selected trace elements (Figure 7B) and trace element ratios (Figure 7C) of primitive CAVAS lavas and for comparison, evolved CAVAS lavas. For further comparison, I also plot primitive MORB (Jenner and O'Neill, 2012) and primitive Mariana (Tamura et al., 2011) and Papuan (Smith et al., 1997; Smith, 2013) arc lavas. In the CAVAS primitive suite, TiO2, FeOt, MgO, and CaO decrease with increasing SiO2 whereas K2O and Na2O increase; Al2O3 and P2O5 show little change (Figure 7A). Compared with their evolved counterpart lavas, the primitive CAVAS lavas range to lower TiO2, FeOt, Na2O, and P2O5 and higher MgO and CaO. The primitive CAVAS basalts are compositionally very similar to primitive MORB in terms of major element concentrations but range to lower TiO2, FeOt, and Na2O and higher CaO. The primitive CAVAS lavas are also very similar to those of the Mariana Arc, the major element compositions of which fall completely within the field of primitive MORB. Primitive lavas of the Papuan Arc exhibit significantly higher TiO2, K2O, and P2O5 than the primitive CAVAS lavas.
Figure 7. SiO2 vs. (A) TiO2, Al2O3, FeOt, MgO, CaO, Na2O, K2O, and P2O5, (B) Sr, Y, Zr, Zr/Y, Nb, Ba, Hf, and Th and (C) Nb/Yb, Ba/Nb, Th/Nb, and Ba/Th, and Th/Nb vs. Ba/Nb and Nb/Yb of primitive and evolved lavas of Sona-Azuero, Golfito and Chagres-Bayano. Shown for comparison are the composition of primitive MORB and primitive lavas of the Marianas and Papuan arcs. Fields of primitive Atlantic and Pacific MORB glasses (Mg# 60–68, MgO = 6.70–9.69 wt. %, n = 204) are from Jenner and O'Neill (2012). Field for primitive lavas of the Mariana Arc are from Tamura et al. (2011) and fields for primitive lavas of the Papuan Arc are from Smith et al. (1997) and Smith (2013). On plots where the Mariana Arc field is covered by symbols, the field is entirely contained within the primitive MORB field.
Plots of SiO2 vs. Sr, Zr, Nb, Hf, Y, Zr/Y, and Th (Figure 7B) also demonstrate striking similarities between primitive CAVAS lavas and primitive Mariana Arc lavas. Ba, as expected, ranges, to higher values in the primitive CAVAS lavas than primitive MORB and, in contrast to the other elements listed immediately above, ranges to values as high as that defined by the primitive Papuan Arc lavas. As mentioned previously, there is no correlation between Ba and LOI which suggests that the Ba contents are the result of subduction additions and not alteration. Interestingly, the primitive CAVAS lavas have significantly lower concentrations of the HFSE (Zr, Nb, Hf) and the “subduction component indicators” Sr, Ba, and Th, than the Papuan suite but much lower Zr/Y which suggests that the former was either derived from a more depleted source or underwent higher degrees of partial melting than the latter.
In Figure 7C, I plot SiO2 vs. Nb/Yb, Th/Nb, Ba/Nb and Ba/Th. Nb/Yb, Ba/Nb, and Ba/Th show no correlation with SiO2 while Th/Nb increases moderately. Nb/Yb is a ratio of two fluid-immobile elements with different compatibilities and highlights mantle depletion (that is, Nb/Yb decreases with increasing source depletion) (Pearce et al., 2005). Ba/Nb, Th/Nb, and Ba/Th are proxies which gauge total, deep and shallow subduction inputs, respectively (Elliot et al., 1997; Pearce et al., 2005). Assuming that melting occurred in the spinel peridotite stability field, the lower Nb/Yb of primitive CAVAS lavas relative to Mariana and Papuan arc lavas suggests either a more depleted source and/or higher degrees of melting of its source, which is consistent with variations in Zr/Y which are generally lower for the primitive CAVAS suite. The primitive CAVAS lavas range to much higher Ba/Nb, Th/Nb, and Ba/Th than the primitive Mariana Arc lavas which demonstrates a higher subduction component in the genesis of the former relative to the latter. Ba/Nb and Ba/Th are also higher in the primitive CAVAS suite relative to the primitive Papuan Arc lavas but Th/Nb is significantly lower in the CAVAS suite. This suggests that the CAVAS source received greater shallow but lesser deep subduction additions than the source responsible for the primitive Papuan Arc lavas.
Plots of SiO2 vs. gauges of fertility and/or degrees of partial melting such as Nb/Yb and Zr/Y (Figures 7B,C) demonstrate that the primitive Chagres-Bayano arc lavas were derived from either a more depleted source or underwent higher degrees of partial melting than primitive lavas of the Sona-Azuero and Golfito arc segments. These plots also demonstrate a more depleted source or higher degree of melting for all primitive CAVAS lavas relative to primitive arc lavas of the Papuan Arc, but a similar source to that of the Mariana Arc in the case of Sona-Azuero and Golfito; Chagres-Bayano extends to more depleted values (lower Nb/Yb and Zr/Y) than primitive lavas of the Mariana Arc. In the Chagres-Bayano primitive basalts, Nb/Yb and Zr/Y range from 0.17 to 1.02 and 1.13 to 3.23, respectively, whereas the Sona-Azuero record Nb/Yb and Zr/Y of 0.97–1.12 and 2.81–3.62; the Golfito primitive basalt yield Nb/Yb and Zr/Y of 0.68–0.99 and 2.21–2.54, respectively.
Subduction Contributions I: Constraints From N-MORB Normalized Plots of Primitive Lavas Normalized to 8 wt.% MgO
Plotted on Figure 8 are: (A) N-MORB normalized patterns of four Sona-Azuero, two Golfito and 15 Chagres-Bayano primitive basalts; (B) N-MORB normalized patterns of the mean of all primitive basalts of Sona-Azuero (n = 6), Golfito (n = 3), and Chagres-Bayano (n = 17) arc segments normalized to 8 wt. % MgO; and (C–E) the mean N-MORB normalized patterns of the primitive Sona-Azuero, Golfito and Chagres-Bayano primitive suites normalized to 8 wt. % MgO (shown in B) highlighting the distinctive mantle, deep subduction and shallow subduction components as outlined by Pearce et al. (2005). Table 3 provides compositions of primitive lavas of Sona-Azuero, Golfito and Chagres-Bayano normalized to 8 wt. % MgO and for comparison, the compositions of Mariana and Papuan arc primitive lavas normalized to 8 wt. % MgO.
Figure 8. N-MORB normalized plots of (A) four Sona-Azuero, two Golfito and fifteen Chagres-Bayano primitive basalts, (B) Sona-Azuero, Golfito and Chagres-Bayano lavas normalized to 8 wt. % MgO and (C–E) the N-MORB normalized patterns of the primitive Sona-Azuero, Golfito and Chagres-Bayano suites normalized to 8 wt. % MgO highlighting the distinctive mantle, deep subduction and shallow subduction components as suggested by Pearce et al. (2005). N-MORB concentrations are from Sun and McDonough (1989).
Table 3. Whole rock compositions of primitive CAVAS, MORB, Mariana Arc and Papuan Arc lavas normalized to 8 wt. % MgO.
In a given subduction system, shallow subduction input is characterized by elements which are mobile in low-temperature aqueous fluids. Such low-temperature mobile elements include Ba, Rb, Sr and Pb. Alternatively, deep subduction is distinguished by source enrichments in both this group of elements as well as the group of melt-mobile incompatible elements. These melt-mobile elements include Th and the LREE, which are mobile at higher temperature or as a result of sediment melting (Pearce et al., 2005).
Perusal of Figure 8 suggests that the primitive Chagres-Bayano suite is the most enriched of the three suites in both shallow subduction and deep subduction components. This is verified in Figure 7C which shows that the primitive Chagres-Bayano lavas extend to higher Ba/Th (shallow subduction gauge) and higher Th/Nb (deep subduction gauge). Ba/Th and Th/Nb range from 117 to 6657 and 0.09 to 0.69 in the primitive Chagres-Bayano basalts whereas the primitive suite of Chagres-Bayano lavas normalized to MgO = 8 wt. % records Ba/Th and Th/Nb of 691 and 0.25 (Table 3). In contrast, Ba/Th and Th/Nb range from a relatively modest 258–414 and 0.11–0.15 in the primitive Sona-Azuero basalts; the primitive suite of Sona-Azuero lavas normalized to MgO = 8 wt. % yields Ba/Th of 315 and Th/Nb of 0.24. Th concentrations are presented in one of two primitive Golfito basalts and records Ba/Th of 352 and Th/Nb of 0.11, within the range of the primitive Sona-Azuero basalts. Primitive Golfito lavas normalized to 8 wt. % MgO record Ba/Th of 294 and Th/Nb of 0.13 (Table 3). Not surprisingly, the primitive Chagres-Bayano basalts also record the highest “total subduction component” with Ba/Nb of 19–594 and a normalized to MgO = 8 wt. % Ba/Nb of 171. The suite of primitive Sona-Azuero and Golfito lavas record much lower Ba/Nb ratios of 21–63 and 40–62 whereas the suite of primitive Sona-Azuero and Golfito lavas normalized to 8 wt. % MgO yield Ba/Nb of 75 and 38, respectively. As the Chagres-Bayano arc segment began to form later (70–39 Ma) than those of the Sona-Azuero (75–39 Ma) and Golfito (75–66 Ma) arc segments (Buchs et al., 2010; Wegner et al., 2011) and the three segments likely represent an originally contiguous system (Montes et al., 2012; Whattam and Stern, 2015), this suggests that the early CAVAS evolved from less to more subduction-modified compositions over time. Enrichment in these subduction components in the primitive Chagres-Bayano basalts relative to primitive basalts of the Sona-Azuero and Golfito complexes reflect a more extensive interaction of hydrous metasomatic fluids or melts which could also have resulted in higher degrees of melting in the Chagres-Bayano basalts relative to those of Sona-Azuero and Golfito as shown above.
Compared with primitive lavas of the Mariana and Papuan arcs, the early primitive CAVAS lavas exhibit greater shallow subduction components (as gauged by Ba/Th) than both Mariana and Papua but a lesser deep subduction component (as gauged by Th/Nb) than the Papuan Arc. Primitive lavas of the Mariana Arc record Ba/Th and Th/Nb of 160–189 and 0.16–0.47 whereas the Papuan Arc primitive lavas record Ba/Th and Th/Nb of 46–163 and 0.33–3.01.
Subduction Contributions II: Constraints From Nb/Yb vs. M Plots
Further insights into the relative contributions of slab-derived subduction zone fluids to the petrogenesis of the early CAVAS lavas can be obtained with plots of M/Yb vs. Nb/Yb (Pearce and Peate, 1995) where M represents the element under study. In such plots, Nb is widely thought to be least effectively transferred from the slab to the mantle wedge melting region (Pearce and Peate, 1995; Peate et al., 1997). According to Pearce and Peate (1995), if adding from the slab a variable M to a mantle wedge source of constant composition, samples will displace from the MORB array to higher M/Yb ratios and form a vertical trend at given Nb/Yb, or plot within the MORB array. Following Pearce et al. (1995), the subduction contribution is quantified by contour lines drawn vertically upward, paralleling the MORB array (Figure 9). The MORB array in this study is as defined by Xia et al. (2012) but essentially defines oceanic basalts. As can be seen in Figure 9, primitive and evolved basalt samples from the Sona-Azuero and Golfito complexes mostly plot within the MORB array and form a pseudo-linear trend that passes through the average N-MORB to average E-MORB composition, suggesting that the mantle contributes ~75% of Nd, Zr, and Th (~6-8 samples out of a total of 24 plot above the array), and nearly 100% of La through the peridotite melting process in the case of Sona-Azuero. In contrast, the compositions of the primitive Chagres-Bayano basalts are instead vertically offset to values much higher than the MORB array, suggesting significant contributions of these elements via slab-derived fluids. For example, the subduction contributions of Th range from <70 to 90% for the primitive Chagres-Bayano basalts and in excess of 90% for the evolved Chagres-Bayano basalts whereas the subduction contributions of La range from 20 to >75% for the primitive and evolved Chagres-Bayano basalts (Figure 9). Also of significance, and as noted earlier, is the difference in Nb/Yb between the Sona-Azuero and Golfito complexes and the Chagres-Bayano complex. Basalts of the Chagres-Bayano complex exhibit significantly lower Nb/Yb than those of the Sona-Azuero and Golfito complexes suggesting either a higher degree of melting or tapping of a more depleted source in the case of the former. Whereas the Sona-Azuero and Golfito lavas are consistent with tapping of a source intermediate to N- and E-MORB, the Chagres-Bayano lavas are instead consistent with partial melting of a source significantly more depleted source than N-MORB.
Figure 9. Comparison of early CAVAS primitive and evolved basalts vs. ocean floor basalts which define the MORB array (see Xia et al., 2012), intra-oceanic arc rocks (Kelemen et al., 2003) and boninites (see Xia et al., 2012 for references) of Cape Vogel (Papua-New Guinea), Site 786 (Izu-Bonin forearc) and Dachadaban (China) in Nb/Yb vs. (A) Th/Yb, (B) La/Yb, (C) Nd/Yb and (D) Zr/Yb space. The solid parallel lines in (A,B) with percentages indicated represent contours of percentage of subduction zone contributions for the particular element [for example, Th in (A) and La in (B)] in the mantle (Pearce et al., 1995; see text for further explanation). Average N-MORB and MORB values are from Arévalo and McDonough (2010) and the E-MORB value is from Sun and McDonough (1989). Abbreviations: Chag-Bay, Chagres-Bayano; DCDB, Dachadaban; Golf, Golfito IOA, intra-oceanic arc; Sona-Az, Sona-Azuero.
Comparison With Global Primitive Arc Melts
A study of a large dataset (n = 938) of primitive arc melts from 30 continental and oceanic arc systems (Schmidt and Jagoutz (2017) recognized six principle primitive arc melt types: calc-alkaline basalts and andesites; tholeiitic basalts; highly depleted tholeiitc andesites; shoshonites; and low-Si basalts. On the basis of K2O vs. SiO2 relations (Figure 10) the mean composition of Sona-Azuero, Golfito and Chagres-Bayano are analogous to depleted tholeiitic andesites, tholeiitic arc basalts to calc-alkaline andesites, and tholeiitic arc basalts, respectively. These mean compositions generally agree with the AFM (total-alkalis, FeOt, MgO) plot (Supplementary Figure 3). Approximately half of the Sona-Azuero primitive and evolved samples plot within the tholeiitic field; apart from one MgO-rich primitive sample, the remaining primitive samples plot within the calc-alkaline field. A similar trend is seen for Golfito. The Chagres-Bayano primitive magmas plot almost completely within the tholeiitic field whereas approximately half of the evolved samples show an Fe-enrichment trend and the other half plot within the calc-alkaline field.
Figure 10. K2O vs. SiO2 for primitive lavas of (A) the Central American Arc, (B) the Sona-Azuero Arc, (C) the Golfito Arc and (D) the Chagres-Bayano Arc. Fields for the oceanic arc systems are from Schmidt and Jagoutz (2017).
In terms of SiO2 vs. MgO, CaO, TiO2, and Na2O (Supplementary Figure 4), global tholeiitic and calc-alkaline oceanic arc basalts show great overlap with each other and depleted tholeiitic andesites plot uniquely due to their higher SiO2 contents. Despite the overlap between tholeiitic and calc-alkaline basalts a broad observation is that primitive magmas of all three complexes plot within the tholeiitic and calc-alkaline fields. Again, this is consistent with the AFM plot (Supplementary Figure 3).
Schmidt and Jagoutz (2017) also plotted average (RbPMN, BaPMN, ThPMN, UPMN, where PMN is primitive mantle-normalized, PM values from Sun and McDonough, 1989) vs. K2O (Figure 11) to assess slab-derived contributions of LILE. Relatively good correlations are shown by the global oceanic tholeiitic arc basalts and calc-alkaline basalts. Although there is no correlation shown by Azuero and Golfito magmas (R2 of 0.07 and 0.18, respectively), excellent correlation is shown by the Chagres-Bayano primitive magmas (R2 = 0.85). The reason for the lack of correlation shown by Azuero and Golfito primitive magmas may simply be the small sample set (n = 5 and 3 for Azuero and Golfito, respectively, whereby Chagres-Bayano has 17 samples). The excellent correlation between average (RbPMN, BaPMN, ThPMN, UPMN) and K2O exhibited by Chagres-Bayano suggests that these LILE (Rb, Ba, Th, U) were derived from the subducting slab.
Figure 11. Average primitive mantle-normalized LILE (Rb, Ba, Th, U) vs. K2O for primitive Sona-Azuero, Golfito and Chagres-Bayano magmas vs. those of oceanic arc systems (Schmidt and Jagoutz, 2017). Abbreviations: Sona-Az, Sona-Azuero; Golf, Golfito; Chag-Bay, Chagres-Bayano.
Mantle Potential Temperature
Potential mantle temperature estimates were calculated with PRIMELT3 (Herzberg and Isamow, 2015) and the method of Putirka (2008). In the former case, using Fe2+/FeT of 0.85 and 0.90, all primitive basalts yielded Tp of <1,305°C which is consistent with ambient and not anomalously hot mantle. In the latter case, similar results were obtained but for the identical calculations of 1,633 ± 47°C for two Sona-Azuero samples (DB05-087 and DB06-112) (Buchs et al., 2010).
The “success” of the these two high Tp may be due to the fact that these two lavas were derived largely from DMM and HIMU mantle rather than from a subduction-modified source; i.e., their formation may have occurred early in the subduction process before influences from the sinking/subducting slab became prominent. An age determination would help confirm this hypothesis but unfortunately is unavailable.
Plume-Subduction Interaction and Tectonic Considerations
Smith et al. (1997) argued that high-Mg arc magmas can breach the crust only in unusual tectonic circumstances and used the Papuan Arc to illustrate this. In the case of the Papuan Arc, impingement of seafloor spreading in the Woodlark Basin upon the Papuan Arc resulted in a unique extensional tectonic regime unlike most volcanic arc systems (Smith et al., 1997; Smith, 2013). Other studies also emphasize the role of an extensional environment and/or thermal anomaly in generating primitive lavas. For example, Bacon et al. (1997) list numerous pieces of evidence to suggest that the uppermost mantle beneath the Cascades of the northwestern US which are responsible for primitive, high-Mg lavas of various volcanic fields of the Cascades Arc is anomalously hot. A hot sub-arc mantle beneath the Cascades is consistent with the young age of the subducting slab, high heat flow (Blackwell et al., 1990), and an extensional environment (Rogers, 1985) of the southern Washington to northern California segment of the Cascades Arc system. Such lithospheric extension, similar to that posited for the Papuan Arc, is consistent with mantle upwelling and, according to Bacon et al. (1997), promotes escape of primary magmas. Similarly, subduction-related high-Mg primitive basalts of southern Sardinia, Italy are ones which formed during crustal thinning within an extension-dominated tectonic setting (Mattioli et al., 2000). In the case of the Sardinian high-Mg magmatism, the extensional deformation and related complex tectonic features have been invoked as a cause for rapid breaching of the crust of primitive magmas (Mattioli et al., 2000). In the Lamongan Volcanic Field of the Sunda Arc, Indonesia, extensional tectonics has created conditions that promoted the rapid ascent of parental magmas (Carn and Pyle, 2001). A myriad of other studies have emphasized the relation between extensional tectonics in volcanic arcs and the eruption of lavas with primitive chemical characteristics (e.g., Luhr and Carmichael, 1981; Knittel and Oles, 1995). In such settings, the development of thinned and fractured crust allows rising magma to erupt at the surface at a relatively unmodified state, rather than ponding at the crust-mantle boundary. The rapid passage to the surface of individual magma batches inhibits the formation of long-lived crustal magma chambers and invariably leads to the formation of monogenetic vent fields comprising tens to thousands of individual eruptive centers, for example, cinder cones and maars, in these environments (e.g., the Michoacán-Guanajuato Volcanic Field, Mexico, Luhr, 1997 and the Macolod Corridor, Philippines, Knittel and Oles, 1995).
To my knowledge, the role of extension is not known in the case of the early CAVAS, but the presence of a sub-arc thermal anomaly at the time of CAVAS establishment is well known. For example, picrites and komatities which require melting of high temperature material ascending within plume conduits comprise numerous segments of the CLIP in Costa Rica (Alvarado et al., 1997), western Columbia (Kerr et al., 1996a, 2002; Arndt et al., 1997; Serrano et al., 2011) and Curaçao (Kerr et al., 1996b; Sinton et al., 1998). Modern-day picrites are derived from mantle with a potential temperature up to 250°C hotter than that which yields MORB (see Hill et al., 1992) and komatiites are derived from even hotter mantle (Campbell et al., 1989; Arndt, 2003). On the basis of petrological modeling, Herzberg and Gazel (2009) demonstrated that the Galapagos Plume, responsible for CLIP formation, had potential temperatures of 1,560–1,620° C in the Cretaceous. Similarly, Hastie and Kerr (2010) showed that primary magmas of the CLIP in Curaçao had ~20% MgO and were derived from 30 to 32% partial melting of a fertile peridotite, the source region of which had a potential temperature of 1,564–1,614°C. CLIP lavas thus were derived from decompression melting of a hot, upwelling mantle plume with excess heat relative to ambient mantle and thus, an unusually hot sub-arc mantle existed immediately preceding and overlapping SI. According to Tatsumi and Maruyama (1989), high geothermal gradients in the mantle wedge resulting from back-arc basin opening and subduction of relatively young and hot oceanic lithosphere can result in the partial melting of hydrous peridotites at shallow levels in the sub-forearc mantle wedge and the production of primary high magnesium andesites. In the case of Central America, it is clear that emplacement of the CLIP substantially raised geothermal gradients in the sub-arc mantle wedge which could have facilitated partial melting of hydrous peridotite to generate the early CAVAS primitive magmas. Furthermore, on the basis of thermodynamic modeling, Gerya et al. (2015) demonstrated that plume-induced subduction initiation (PISI) results in mechanical weakening and thinning of the lithosphere. All of the aforementioned factors would facilitate either primitive magma formation or their rapid ascent through the crust.
It is well known that there exists a chemical, isotopic and temporal relation between the CLIP and early CAVAS products (e.g., Hauff et al., 2000a; Hoernle et al., 2004; Wegner et al., 2011) suggesting a genetic link between the two. These studies demonstrate an almost complete overlap in terms of Pb and Nd between early primitive CAVAS lavas and those of the CLIP and Galapagos Plume.
Via plots of 143Nd/144Nd vs. 206Pb/204Pb and 207Pb/204Pb, Allibon et al. (2008) showed that formation of Late Cretaceous to Paleocene arc sequences along western Ecuador required three component mixing of depleted MORB mantle (DMM, East Pacific Cretaceous MORB), HIMU (carried by the CLIP) and an enriched, slab-derived pelagic sediment and chert component. These Ecuadorian arc sequences are ones considered by Whattam and Stern (2015) to represent the same plume-induced volcanic arc activity as in Central America. Using the 143Nd/144Nd vs. 206Pb/204Pb plot of Allibon et al. (2008), I show in Figure 12 that formation of both CAVAS lavas and the CLIP require mixing of the same three components. Allibon et al. (2008) suggested that an average contribution of 12–15% HIMU, 7–15% sediments and chert and 70–75% DMM is required to explain the Pb and Nd isotopic values. Allibon et al. (2008) further suggested that an anomalously high thermal regime responsible for such high proportions of HIMU was likely inherited from the CLIP which supports the idea of an elevated thermal regime at subduction inception.
Figure 12. Tripolar mixing model using initial 206Pb/204Pb vs. initial 143Nd/144Nd for the Sona-Azuero, Chagres-Bayano and Golfito complexes (Allibon et al., 2008). For references for the various fields (that is, DMM, HIMU, pelagic sediments and chert), see Allibon et al. (2008). The field for the Galapagos Plume at 90 Ma is from Hauff et al. (2000b) and the isotope data for Sona-Azuero, Golfito and Chagres Bayano are from Hauff et al. (2000a), Lissinna (2005) and Wegner et al. (2011). Abbreviations: Sona-Az, Sona-Azuero; Golf, Golfito; Chag-Bay, Chagres-Bayano.
In addition to melting of the mantle, arrival of the CLIP plume head and an anomalously hot sub-arc mantle beneath the burgeoning CAVAS (Figure 13) could help explain the ascent of primitive magmas directly from the asthenosphere (Figure 13). Moreover, in other cases the arrival of a plume head has been invoked as a direct cause of crustal weakening and lithospheric extension (Hill et al., 1992) and the production of primitive lavas. For example, arrival of the Yellowstone Plume at 16–15 Ma has been invoked as the trigger for lithospheric extension accompanying eruption of the Columbia River Flood Basalts (Parsons et al., 1994; Hooper, 1997). I suggest that arrival of the Galapagos head plume at the base of the Farallon Plate led to lithospheric extension in addition to mechanical weakening and thinning of the lithosphere (Gerya et al., 2015) which allowed for production and rapid ascent of a high percentage of primitive magmas which comprise the early CAVAS. It is also noteworthy that such a model is consistent with either a collision-induced (Buchs et al., 2010) or PISI scenario (Figure 13, Whattam and Stern, 2015).
Figure 13. Cartoon depicting the generation of primitive magmas via plume induced subduction initiation. Modified from Whattam and Stern (2015).
Conclusions
Primitive lavas with Mg ≥60 and concentrations of Ni and Cr extending to greater than 300 ppm and 700 ppm, respectively, are identified from the Sona-Azuero, Golfito and Chagres-Bayano arc segments of the early (75–39 Ma) CAVAS. Radiometric ages are limited but production of primitive magmas appears to be restricted to between 71 and 66 Ma but other considerations suggests SI circa 89 Ma which suggests primitive magma production for circa 20 m.y. In terms of major element abundances, the early CAVAS primitive lavas are very similar to primitive MORB and primitive arc basalts of the Mariana Arc system. In terms of most trace elements, the early CAVAS primitive lavas are also similar to those of the Mariana Arc and to global intra-oceanic arc tholeiitc basalts and calc-alkaline basalts. With respect to subduction components, primitive basalts of Chagres-Bayano exhibit evidence of significantly higher shallow and deep subduction components as gauged by Ba/Th and Th/Nb than primitive basalts of Sona-Azuero and Golfito. A plot of average (RbPMN, BaPMN, ThPMN, UPMN) vs. K2O demonstrates that these LILE (Rb, Ba, Th, U) were derived from the subducted slab in the case of the Chagres-Bayano complex.
As has been shown in previous studies, early CAVAS lavas are remarkably similar in isotopic composition to those of the CLIP oceanic plateau. In 143Nd/144Nd vs. 206Pb/204Pb space, almost all primitive and evolved lavas of the early CAVAS segments in Sona-Azuero, Golfito and Chagres-Bayano plot within the fields defined by the Galapagos Plume at 90 Ma. All early CAVAS lavas are consistent with formation from a source composed of three principal components: depleted MORB mantle (DMM), a HIMU component carried by the CLIP, and subducted pelagic sediments and chert. These isotopic similarities between plume and arc lavas are consistent with subduction-plume interaction regardless of whether subduction inception was collision- or plume-induced.
Subduction-plume interaction also dictates that an elevated sub-arc thermal anomaly was present at inception of the CAVAS. Evidence of an elevated thermal anomaly are provided by high-MgO picrites and komatiites which comprise integral components of the CLIP, as they require high temperatures (>1,550°C) of formation. Relatedly, potential temperatures of 1,633 ± 47°C were calculated for two Sona-Azuero samples, which suggest the existence of anomalously hot mantle during early SI. I suggest that, in addition to providing an anomalously high temperature regime in the sub-arc mantle at inception of the CAVAS, extrusion of the CLIP oceanic plateau also resulted in lithospheric weakening and extension which allowed for production and rapid ascent of primitive magmas which comprise the early CAVAS.
Author Contributions
The author confirms being the sole contributor of this work and approved it for publication.
Conflict of Interest Statement
The author declares that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Acknowledgments
SW acknowledges financial support from the Smithsonian Tropical Research Institute, Balboa, Ancon, Panama during his postdoctoral tenure there.
Supplementary Material
The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2018.00114/full#supplementary-material
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Keywords: primitive magmas, volcanic arc, mantle plume, subduction, Central America
Citation: Whattam SA (2018) Primitive Magmas in the Early Central American Volcanic Arc System Generated by Plume-Induced Subduction Initiation. Front. Earth Sci. 6:114. doi: 10.3389/feart.2018.00114
Received: 30 March 2018; Accepted: 26 July 2018;
Published: 03 September 2018.
Edited by:
Oliver Jagoutz, Massachusetts Institute of Technology, United StatesReviewed by:
Marc-Antoine Longpré, Queens College (CUNY), United StatesJ. Gregory Shellnutt, National Taiwan Normal University, Taiwan
Copyright © 2018 Whattam. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Scott A. Whattam, c2F3aGF0dGFAZ21haWwuY29t