February 2022 LIP of the Month

Mafic dyke swarms of Brazil: summary and highlights

Pedro C. Pessano^a,b*, Carlos E. Ganade^b, Miguel Tupinambá^c, Wilson Teixeira^d

^aDepartment of Geophysics, National Observatory, R. Gal. José Cristino, 77, 20921-400 Rio de Janeiro, RJ, Brazil

^bCenter for Applied Geosciences, Geological Survey of Brazil, Av. Pasteur, 404, 22290-240 Rio de Janeiro, RJ, Brazil

^cFaculty of Geology, Rio de Janeiro State University, Rua São Francisco Xavier, 524, 20550-900 Rio de Janeiro, RJ, Brazil

^dInstitute of Geosciences, University of São Paulo, Rua do Lago, 562, 05508-080 São Paulo, SP, Brazil

*Corresponding author at: Department of Geophysics, National Observatory, R. Gal. José Cristino, 77, 20921-400 Rio de Janeiro, RJ, Brazil.

E-mail address: ppessano@gmail.com (P. Pessano)

Extracted from:

Pessano, P. C., Ganade, C. E., Tupinambá, M., Teixeira, W. (2021). Updated map of the mafic dike swarms of Brazil based on airborne geophysical data. Journal of South American Earth Sciences, v. 107, 103076. https://doi.org/10.1016/j.jsames.2020.103076.

1. Introduction

The magmatic record of Brazil spans from the Archean to the Cenozoic (Fig. 1). These episodes occur as dykes, sills, and flood basalts, and are related to relevant extensional events, although some are linked to extension/transtension domains within regional compressive zones. Most of these events date to the Precambrian; nonetheless, the largest records are those of the Phanerozoic, mainly the Mesozoic ones.

Identification of mafic dyke swarms and LIPs (Large Igneous Provinces) are of vital importance in geologic history because they provide information on geodynamics, mantle geochemistry, and paleomagnetism, key information for paleogeographic reconstructions with the aid of barcode matches and precise radiometric ages. Considering such issues, the Brazilian Precambrian shield can be used as a case for refining the cartography of the relevant intraplate activity (e.g., dykes, sills, flood basalts) in space and time. Also, LIPs may have an influence on the global climate, including extinction events, as recorded by the global stable isotopic excursions (Ernst et al., 2020a; 2020b; Ernst and Youbi, 2017; Ernst, 2014, and references therein) and changes in sedimentary composition (Zhang et al., 2018). Figure 2 exhibits the temporal distribution of mafic dyke swarms and LIPs in Brazil, along with their associated secular change.

In this web piece, we present an updated map of the mafic dyke swarms of Brazil with a closer look at the mysterious shape of the Rio Ceará-Mirim dyke swarm. This event is closely related to the opening of the Equatorial Atlantic and thus, understanding this process, its causes and implications is a matter of great importance. More details on how the map was elaborated, barcode matches, and more illustrations can be found in the original paper.

2. Updated map of the mafic dyke swarms of brazil

Figure 1 – Updated mafic dyke swarms map of Brazil. This map exhibits the main cratonic terranes, mobile belts, sedimentary basins, and the cataloged mafic dyke swarms and magmatic suites and/or formations. In addition, we highlighted the Cretaceous Serra Geral Flood Basalts within the Paraná Basin. The Arabic numerals refer to cataloged dyke swarms, and the Roman numerals indicate magmatic suites and/or formations (see Table 1, Table 2, and Supplementary Material for further details). AR: Argentina, BO: Bolivia, CO: Colombia, GY: Guianas, GF: French Guiana, PY: Paraguay, PE: Peru, SR: Suriname, UY: Uruguay, VE: Venezuela. Extracted from Pessano et al. (2020). For full details, see the original article.

Table 1 – Mafic dyke swarms of Brazil (see notes at bottom of table).

ID	Unit	Trend	Period	Age (Ma)	Method	LIP/Event	References
1	Arraial do Cabo	N50E, N30W	Paleogene	55	Ar-Ar		13, 9
2	Riacho do Cordeiro	N40-60E	Cretaceous	119 ± 2	K-Ar	EQUAMP^L	54
3	Canindé	N60E, N25-50W	Cretaceous	135 - 120	K-Ar	EQUAMP^L	54
4	Rio Ceará-Mirim	N20-85E	Cretaceous	145 - 120	K-Ar	EQUAMP^L	54, 34, 3
5	Coronel João Sá	N25-45E	Cretaceous	212 - 103	Rb/Sr, Ar/Ar	EQUAMP^L	26, 11
6	Serra do Caiapó	N30-55E	Cretaceous	130	K-Ar/Ar-Ar	Paraná-Etendeka^L	28, 3
7	Transminas	N25-45E, N25-65W	Cretaceous	130	Ar-Ar	Paraná-Etendeka^L	42, 30, 13
8	Ponta Grossa	N30-70W	Cretaceous	133	K-Ar/Ar-Ar	Paraná-Etendeka^L	50, 36, 27
9	Serra do Mar	N10-80E	Cretaceous	134	K-Ar/Ar-Ar	Paraná-Etendeka^L	43, 42, 30, 27
10	Florianópolis	N15-80E	Cretaceous	134.1 ± 0.9	U-Pb^T	Paraná-Etendeka^L	50, 36
11	Vitória-Colatina	N10-60W	Cretaceous	136 - 128	Ar-Ar	Paraná-Etendeka^L	43, 42, 3
12	Penatecaua	N15-75E, N20-70W	Jurassic	148 ± 6	K-Ar	Penatecaua^L	32, 8, 3
13	Apoteri	N50-60E	Jurassic	149.5 ± 0.3, 153 ± 0.9	Ar-Ar^SH	Takutu^E	32, 14
14	Cururu	N10-30E, N50-60W	Jurassic	180 ± 9	K-Ar	CAMP^L	8
15	Periquito	N0-60E, N05-65W	Jurassic	192 ± 3	Ar-Ar, K-Ar	CAMP^L	58, 29
16	Carajás	N20E, N40-45W	Jurassic	199.3 ± 0.3	U-Pb^Sp	CAMP^L	58
17	Mosquito Fm.	N65-80E	Jurassic	200	Ar-Ar	CAMP^L	54
18	Laranjal	N05-75E, N05-60W	Jurassic	200	Ar-Ar	CAMP^L	31, 22
19	Rio Trombetas	N05-10E, N50-70W	Jurassic	200	K-Ar	CAMP^L	3
20	Taiano	N15-65E	Jurassic	200	Ar-Ar^SH	CAMP^L	32, 14
21	Cassiporé	N05-80E, N0-60W	Jurassic	202 ± 2	Ar-Ar	CAMP^L	58, 38, 37, 3
22	Uaraná	N35-90E, N05-60W	Jurassic	202 ± 5	U-Pb	CAMP^L	51, 32
23	Rio Pajéu	N05-60E	Jurassic	215 - 170	Field relations	CAMP^L	45, 39, 23
24	Piranhas	N10-70E, N15-65W	Cambrian	507 ± 4	U-Pb^Sp	Piranhas^E	8
25	Fundão	N10-20W	Cambrian	498 ± 16, 525 ± 10	U-Pb^{Sp, LA}		43, 35
26	Itabaiana	N10-55W	Cambrian	525 ± 5	Ar-Ar^SH		48, 35, 21, 17, 15
27	Parauapebas	N0-15E	Cambrian	535.1 ± 0.9	U-Pb^Sp	535 Ma^E	58
28	Conceição-Santana do Araguaia	N05-50W, N0-50W	Ediacaran	565 ± 6 - 480 ± 22	K-Ar	535 Ma^E	47, 2
29	Itabuna-Itaju do Colônia	N25-70E, N10-35W	Cryogenian	676 ± 5, 665 ± 25	U-Pb, Rb-Sr		7, 1
30	Pará de Minas III	N50-60W	Tonian	766 ± 36	U-Pb^T	Gannakouriep^L	59, 41, 30, 13, 3
31	Formiga	N25-90E	Tonian	906 ± 2, 896 ± 11	U-Pb	Bahia-Gangila^L	59, 52, 30, 13
32	Salvador	N15W	Tonian	924.2 ± 3.8	U-Pb^T	Bahia-Gangila^L	52, 49, 44, 11
33	Ilhéus-Olivença	N40-90E, N25-85W	Tonian	926.1 ± 4.6	U-Pb^T	Bahia-Gangila^L	52, 49, 44, 11
34	Rio Perdido	N45-90E	Stenian	1110.7 ± 1.4	U-Pb^T	Rincón del Tigre-Huanchaca^L	58, 57
35	Seringa	N05-75E, N10-80W	Stenian	1079 ± 18	K-Ar	Cachoeira Seca^E	57, 56, 8
36	Siriquiqui	N05-60E, N10-40W	Stenian	1164 ± 23	K-Ar	Cachoeira Seca^E	8
37	Tapuruquara	N45-90E	Stenian	1172 ± 8	U-Pb^Sp	Cachoeira Seca^E	57, 32
38	Cachoeira Seca	N15-90E	Stenian	1186 ± 13	U-Pb^Sp	Cachoeira Seca^E	57, 8
39	Nova Floresta	N25-80E	Stenian	1201 ± 2	Ar-Ar	Cachoeira Seca^E	57, 8
40	Nova Lacerda	N45-55W	Ectasian	1387 ± 17	U-Pb^T	1.4 Ga^E	57, 40
41	Espinhaço	N0-20E, N0-20W	Calymmian, Jurassic	1496 ± 3.2; 193 ± 4	U-Pb^LA, K-Ar		49, 16, 4, 3
42	Chapada Diamantina	N10-70W	Calymmian	1501 ± 9.1	U-Pb		33, 11
43	Curaçá	N25-60E	Calymmian	1506.7 ± 6.9	U-Pb		33, 11
44	Mata-Matá	N40-70E	Calymmian	1576 ± 4	U-Pb^Sp		57
45a	Pará de Minas II	N50-60W	Statherian	1714 ± 5, 1736 ± 36	U-Pb^T	1.79 – 1.75 Ga^L	59, 41, 30, 13, 3
45b	Pará de Minas I	N50-60	Statherian	1791 ± 7, 1798 ± 4	U-Pb^T	1.79 – 1.75 Ga^L	59, 41, 30, 13, 3
46	Januária	N05-55W	Statherian	1762 ± 2	U-Pb^T	Timpton^L	53, 30, 13
47	Quarenta Ilhas	N20-70E, N30-65W	Statherian	1780 ± 3	U-Pb^Sp	Avanavero^L	57, 32, 12
48	Crepori	N15-55E	Statherian	1780 ± 7	U-Pb^Sp	Crepori^E	57, 8
49	Taxista Gabbro	N30-55E	Orosirian	1859 ± 15	U-Pb^Sp	Uatumã^S	57
50	Uraricaá	N40-65W	Orosirian	1882 ± 4	U-Pb^Sp	Uatumã^S	57, 32
51	Tucumã	N15-70W	Orosirian	1882 ± 9	U-Pb^Sp	Uatumã^S	58, 46
52	Carajás	N40-70E, N30-80W	Orosirian	1884.6 ± 1.6	U-Pb^Sp	Uatumã^S	58
53	Ingarana	N20-50E	Orosirian	1893 ± 10	U-Pb^Sp	Uatumã^S	57, 8
54	Feira de Santana	N0-50W	Rhyacian	2100	Field relations		11, 26
55	Crixás-Goiás	N15-70E, N10-80W	Rhyacian	2170 ± 17	U-Pb		19, 18, 10, 3
56	Paraopeba	N15-30E, N10-75W	Rhyacian	2189 ± 45	Rb-Sr		30, 20, 13
57	Aroeira	N05-65E, N20-40W	Rhyacian	2200	Field relations		33, 26, 24, 11
58	Juazeiro and Sobradinho	N0-40E, N10-45W	Rhyacian	2300 - 2051	Field relations		26, 11
59	Lavras	N30-60W	Neoarchean	2658 ± 44, 2551.1 ± 9.8	Sm-Nd, U-Pb		59, 30, 13, 6, 5, 3
60	Uauá	N0-60E, N10-45W	Neoarchean	2726.2 ± 3.2, 2623.8 ± 7	U-Pb		55, 25, 11
Notes for Table 1. The azimuth (Trend) corresponds to the arithmetic mean of the dykes directions. SH: Step heating, LA: LA-ICP-MS, Sp: SHRIMP, T: TIMS, E: Magmatic Event, L: LIP, S: SLIP. 1) Cordani et al. (1974), 2) Gorayeb (1981), 3) Sial et al. (1987), 4) Dossin et al. (1995), 5) Pinese et al. (1995), 6) Pinese (1997), 7) Teixeira et al. (1997), 8) Santos et al. (2002), 9) Bennio et al. (2003), 10) Corrêa da Costa (2003), 11) Dalton de Souza et al. (2003), 12) Santos et al. (2003), 13) Chaves & Neves (2005), 14) Reis et al. (2006), 15) Trindade et al. (2006), 16) Teixeira (2008), 17) Almeida & Hollanda (2009), 18) Corrêa da Costa et al. (2010), 19) Jost & Scandolara (2010), 20) Chaves (2011), 21) Guimarães (2011), 22) Klein & Lopes (2011), 23) Macambira & Ricci (2011), 24) Piaia (2011), 25) Oliveira (2011), 26) Leal et al. (2012), 27) Tomba (2012), 28) Almeida et al. (2013), 29) Costa et al. (2013), 30) Chaves (2013), 31) Klein et al. (2013), 32) Reis et al. (2013), 33) Silveira et al. (2013), 34) Castro (2014), 35) Fleck (2014), 36) Florisbal et al. (2014), 37) Rosa-Costa et al. (2014), 38) Barbosa & Chaves (2015), 39) Barros & Besser (2015), 40) Teixeira et al. (2015), 41) Cederberg et al. (2016), 42) Coelho (2016), 43) Coelho & Chaves (2016), 44) Evans et al. (2016), 45) Macambira et al. (2016), 46) Silva et al. (2016), 47) Gorayeb et al. (2017), 48) Guimarães et al. (2017), 49) Moreira (2017), 50) Florisbal et al. (2018), 51) Baratoux et al. (2019), 52) Chaves et al. (2019), 53) Chaves & Rezende (2019), 54) Hollanda et al. (2019), 55) Salminen et al. (2019), 56) Simões et al. (2019), 57) Teixeira et al. (2019a), 58) Teixeira et al. (2019b), 59) Caxito et al. (2020). For full details, see the original article.

Table 2 – Suites and formations that correspond to important events of intrusive mafic magmatism on the Brazilian Platform (see notes at bottom of table).

ID	Unit	Period	Age (Ma)	Method	Event	References
I	Tapirapuã	Jurassic	196.6 ± 1.8	Ar-Ar^IH	CAMP^L	5, 1
II	Anari	Jurassic	198 ± 0.8	Ar-Ar^IH	CAMP^L	5, 1
III	Pedro Lessa Suite	Tonian	940 ± 42	U-Pb^T	Bahia-Gangila^L	12, 9
IV	Rio Branco Suite (RO)	Stenian	1110 ± 10	U-Pb^T	Rincón del Tigre-Huanchaca^L	13, 4, 2
V	Indiavaí Suite	Calymmian	1416 ± 7	U-Pb^T	1.4 Ga^E	13, 7
VI	Rio Branco Suite (MT)	Calymmian	1423 ± 2	U-Pb^T	1.4 Ga^E	13, 6, 3
VII	Figueira Branca Suite	Calymmian	1426 ± 8	U-Pb^T	1.4 Ga^E	13, 7, 6
VIII	Salto do Céu Gabbro	Calymmian	1439 ± 4	U-Pb^T	1.4 Ga^E	13, 11, 6
IX	Avanavero Dolerite	Statherian	1794.5 ± 1.6; 1787 ± 14; 1782 ± 3	U-Pb^T&Sp	Avanavero^L	10, 8, 2
X	Estrutura Suite	Statherian	1800 - 1600	Field relations		10, 8
Notes for Table 2. Suites and formations that correspond to important events of intrusive mafic magmatism on the Brazilian Platform. IH: Incremental Heating, T&Sp: TIMS & SHRIMP, T: TIMS, E: Magmatic Event, L: LIP. 1) Marzoli et al. (1999), 2) Rizzotto et al. (2002), 3) Geraldes et al. (2004), 4) Rizzotto et al. (2004a), 5) Rizzotto et al. (2004b), 6) Ruiz (2010), 7) Teixeira et al. (2011), 8) Reis et al. (2013), 9) Fonseca (2014), 10) Holanda et al. (2014), 11) Teixeira et al. (2015), 12) Chaves et al (2019), 13) Teixeira et al. (2019a). For full details, see the original article.

The most frequent dyke records in the Brazilian territory are related to the Proterozoic (Figs. 1, 2; Table 1), related to intraplate episodes and LIPs/SLIPs, roughly contemporary or slightly younger than the orogenic processes that built the continental crust (Teixeira et al., 2019a). This finding corroborates with the proposal of Halls (1982), who suggested a relationship between magmatism and the higher geothermal gradient at that time to anomalies in the mantle convection. In other words, this Eon registers an abundance of continental swarms when compared to the Phanerozoic. The younger records, in general, are magmatic episodes linked with the opening of the Atlantic Ocean and fragmentation of the Gondwana (Marzoli et al., 1999, 2018; Hollanda et al., 2019).

Another interesting point is the relative absence of mafic magmatism in the Paleozoic Era and the beginning of the Mesozoic in the South American Platform (Fig. 2). During this interval, large continental masses were converging to form the Pangea Supercontinent in the Upper Permian (Young et al., 2019, and references therein), while sedimentation was occurring in the Brazilian intracratonic Paleozoic basins (Schobbenhaus and Brito Neves, 2003). The records partially confirm the expected: large mafic dyke swarms - the onset of LIPs and/or SLIPs - and the formation of supercontinents tend to alternate over the geological time (Ernst and Bleeker, 2010). Only one Cryogenian unit was identified (site 29; Fig. 1), though it is probably biased due to the data compilation.

The Phanerozoic magmatic record of Brazil is marked by two main events. The first occurred in the Cambrian and is the result of extensional/transtensional movements in the crust after the Brasiliano Event. The second took place in the Mesozoic and is related to the opening processes of the Atlantic Ocean.

Mesozoic magmatism is closely related to the opening process of the Atlantic Ocean and consists of large circumferential, radial, and rectilinear dyke swarms. Three magmatic pulses define the Brazilian Mesozoic magmatism. The first event, the Central Atlantic Magmatic Province (CAMP), occurred around 200 Ma in northern South America and marks, as indicated by its name, the opening of the Central Atlantic Ocean (Marzoli et al., 1999, 2018). The second episode - the Paraná-Etendeka Magmatic Province (PEMP) - took place in southern-southeastern Brazil around 135 Ma and registers the onset of the South Atlantic opening (Renne et al., 1992; Peate 1997; Ernst and Buchan, 1997).

The third and final pulse – recently named as Equatorial Atlantic Magmatic Province (EQUAMP, Hollanda et al., 2019) or Borborema LIP (Matos, 2021) – contributed to the opening of the Equatorial Atlantic in northeastern Brazil at approximately 125 Ma (Holland et al., 2019). Different from the other Mesozoic swarms, this one exhibits a curious shape that will be discussed below.

3. The arcuate shape of the rio ceará mirim dykes: does it represent a circumferential swarm?

Buchan and Ernst (2018, 2019) suggest that the semi-arch pattern of the Rio Ceará-Mirim (site 4; Figs. 1, 3) dykes can be related to a couple of reasons: i) changes in the stress fields of the crust, or ii) posterior deformation. There were no major deformational events in that region after the Cretaceous, so the most plausible hypothesis is that of changes in the crustal stress field. This idea corroborates with Oliveira (1992), who suggested that the minimum compressive stress axis changed from NW-SE to N–S around the Potiguar Basin. Alternatively, Matos (1992) proposed a clockwise rotation of the least-principal compressive stress north of the Patos Shear Zone. Thus, considering the structural geology of the Borborema Province (NE Brazil), where the most notable arching occurs, the dykes possibly followed, in part, some local E-W trending shear zones (e.g., Patos shear zone), and then cut at quasi-normal angles those that occur within each tectonic domain.

Figure 2 – Chronostratigraphic chart of the intrusive mafic records (arrows), major and minor Phanerozoic extinction events (red and green crosses, respectively), LIPs and/or magmatic events (stars) from the Neoarchean in which the oldest dykes of Brazil are found, to the Paleogene, most recent period with a cataloged mafic record. A: Archean, Cz: Cenozoic, O: Ordovician, Tr: Triassic; a: Eocene-Oligocene Extinction (33.9 Ma), b: End-Cretaceous Extinction (66.0 Ma), c: Cenomanian-Turonian Extinction (93.9 Ma), d: Early Toarcian Extinction (182.7 Ma), e: End-Triassic Extinction (201.3 Ma), f: Cambrian-Ordovician Extinction (488 Ma). Extinction events from Ernst et al. (2020) and Ernst and Youbi (2017). For full details, see the original article.

Conversely, instead of the acquired arcuate shape, this circumferential geometry may be an original feature. As described by Buchan and Ernst (2019), circumferential swarms have approximately circular or elliptical shapes with diameters from hundreds to thousands of kilometers. The diameters are seen to influence the width of the dykes, as Buchan and Ernst (2019) noticed that the larger the diameter, the larger the dyke widths. Giant circumferential dyke swarms (diameters of 1500–2500 km) commonly form a coupled system with radiating dykes (e.g., PEMP and High Arctic Large Igneous Province, HALIP, dykes), which may indicate their plume origin (Buchan and Ernst, 2018, 2019). Buchan and Ernst (2019) propose that these circular geometries correspond to the edges of flattened plume heads and occur along the margins of the associated domal uplifts. One hypothesis is that the geometrical center of these circumferential dykes could constitute a plume center that would be placed at southern Gabon (Fig. 3). However, to date, no volcanic record has been reported in this area, and no mapping of the continuation of these dykes in equatorial Africa is available. Buchan and Ernst (2019) classify the PEMP dykes in Brazil and Namibia as a giant circumferential dyke swarm. In Brazil, the Ponta Grossa swarm (site 8; Figs. 1, 3) is perpendicular to the Serra do Mar and Florianópolis dykes (sites 9 and 10, respectively; Figs. 1, 3). These dykes are also intersected at quasi-right angles by some sparse sets that constitute the circumferential shape (Buchan and Ernst, 2019, Fig. 3). Buchan and Ernst (2019) did not include the EQUAMP/Borborema LIP dykes into this classification, probably due to the age difference - PEMP is ca. 135 Ma, while EQUAMP is ca. 130 Ma (Hollanda et al., 2019) - and different hotspots, PEMP is related to the Tristan da Cunha (Ernst and Buchan, 1997; Peate, 1997), and the EQUAMP/Borborema LIP is probably linked to the St. Helena (Matos et al., 2021; Archanjo et al., 2002; Steinberger, 2000; O’Connor and Le Roex, 1992). Nevertheless, despite the mentioned differences, both magmatic provinces could constitute one giant circumferential South Atlantic Magmatic Province in which the equatorial mafic swarms represent a later event.

Figure 3 – 130 Ma reconstruction of the South American and African Plates according to Müller et al. (2019). This map exhibits Jurassic and Cretaceous mafic records identified in Brazil and some Mesozoic mafic dyke in the African counterpart. The stars show the possible plume heads based on the orientation of the dikes. The circles highlight the arcuate pattern of Cretaceous dyke in northeastern and southeastern Brazil, as well as estimate the area of the EQUAMP swarm if it constitutes a circumferential swarm. The location and age of HOD and Okavango swarms are from Trumbull et al. (2004) and Trumbull et al. (2007). Am: Amazonian Craton, Cg: Congo Craton, Ka: Kalahari Craton, SF: São Francisco Craton, WA: West African Craton; HOD: Henties-Bay-Outjo dyke swarm. For full details, see the original article.

However, the issue of classifying the Rio Ceará-Mirim dykes as being a part of a larger circumferential swarm is that, as mentioned, we did not find any Cretaceous dykes in the African counterpart (Fig. 3), and the absence of accurate dating. High-precision U–Pb dating of the EQUAMP swarms would represent a great leap in classifying these dykes (Buchan and Ernst, 2019). It would permit us to correlate them with the Paraná-Etendeka records, as the Transminas segment (site 7) extends towards the Rio Ceará-Mirim southwestern branch (Figs. 1, 3). Based on the available data, it seems plausible that their semi-arch shape is due to the mentioned change in the stress field (Oliveira, 1992; Matos, 1992).

References

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