Central Atlantic Magmatic Province

The Central Atlantic magmatic province (CAMP) was formed during the breakup of Pangaea during the Mesozoic Era. The initial breakup of Pangaea in early Jurassic time provided a legacy of basaltic dikes, sills, and lavas over a vast area around the present central North Atlantic Ocean.

Connected magma flows

Although some connections among these basalts had long been recognized, in 1988 they were linked as constituting a single major flood basalt province^{(Rampino and Stothers)}. The basaltic sills of similar age (near 200 Ma, or earliest Jurassic) and composition (intermediate-Ti quartz tholeiite) which occur across the vast Amazon River basin of Brazil were linked to the province in 1999^{(Marzoli et al.)}.

Geographical extent

The province has been described as extending within Pangaea from present-day central Brazil northeastward about 5000 km across western Africa, Iberia, and northwestern France, and from the interior of western Africa westward for 2500 km through eastern and southern North America^(McHone).

If not the largest Province by volume, the CAMP certainly encompasses the greatest area known, roughly 11 million km², of any continental large igneous province.

Nearly all CAMP rocks are tholeiitic in composition, with widely separated areas where basalt flows are preserved, as well as large groups of diabase (dolerite) sills or sheets, small lopoliths, and dikes throughout the province.

Dikes occur in very large individual swarms with particular compositions and orientations. CAMP activity is apparently related to the rifting and breakup of Pangaea during the Late Triassic through Early Jurassic periods, and the enormous province size, varieties of basalt, and brief time span of CAMP magmatism invite speculation about mantle processes that could produce such a magmatic event as well as rift a supercontinent^{(Wilson; McHone)}.

Connection with the T-J boundary and the associated mass-extinction event

Since this argument is still debated within the geological community, it seems a good choice to present the two main points-of-view. One hypothesis is based especially on studies on Triassic-Jurassic basins from Morocco where CAMP lava flows are outcropping^{(e.g., Marzoli et al., 2004)}, whereas the other is based on data from eastern North American basins and lava flows^{(Whiteside et al., 2007)}, respectively.

Morocco

Introduction

The thickest lava flow sequences of the African CAMP are situated in Morocco, where we can find more than 300 metres thick basaltic lava piles. The most studied area is Central High Atlas, where the best preserved and most complete basaltic lava piles are exposed. According to geochemical, petrographic and isotopic data four distinct tholeiitic basaltic units were recognized and can be placed throughout the Central High Atlas: Lower, Intermediate, Upper and Recurrent basaltis. The Lower and Intermediate units are constituted by Basaltic Andesites, whereas the Upper and Recurrent units have basaltic composition. From Lower to Recurrent unit, we observe:
*a progressive decrease of eruption rate (the Lower and the Intermediate units represent over 80 % of preserved lava volume);
*a trend going from intersertal to porphyric petrographic texture;
*a progressive depletion of incompatible element contents in the basalts, possibly linked to a progressive depletion of their mantle source.

Isotopic analyses

Ages were determinated by ⁴⁰Ar/³⁹Ar analysis on Plagioclase^{(Knight et al., 2004; Marzoli et al., 2004; Verati et al., 2007)}. These data show undistinguishable ages (199.5 +/- 0.5 Ma.) from Lower to Upper lava flows, from central to northern Morocco. Therefore the CAMP is an intense and short magmatic event. Basalts of the Recurrent unit are slightly younger (mean age: 197 +/- 1 Ma) and represent a late event. Consistently, the Upper and Recurrent basalts are separated by a sedimentary layer, that locally reaches thickness of circa 80 m.

Magnetostratigraphy

According to magnetostratigraphic data, the Moroccan CAMP were divided into five groups, differing in p-mag directions (declination and inclination)^{(Knight et al., 2004)}. Each group is composed by a smaller number of lava flows (i.e., a lower volume) than the preceding one. These data suggest that the CAMP were created by five short magma pulses and eruption events, each one possibly <400 (?) years long. All lava flow sequences are characterized by normal polarity, except for a brief paleomagnetic reversal yielded by one lava flow and by a localized interlayered limestone in two distinct section of the High Atlas CAMP.

Palynological analyses

Palynological data from sedimentary layers samples at the base of four lava flow sequences constrain the onset of the CAMP, since there is no evidence of depositional hiatus or tectonic deformation at the bottom of the lava flow piles^{(Marzoli et al., 2004)}. The palynological assemblage observed in these basal layers is typical of Late Triassic age, similar to that of the uppermost Triassic sedimentary rocks of eastern North America^{(Fowell and Traverse, 1995)}.Samples from interlayered limestone in lava flows provided unreliable palynological data. In fact only one limestone bed from the top to the central High Atlas upper basalts yielded a Late Triassic palynological assemblage. However, the observed sporomorphs in this sample are rare and poorly preserved.

Conclusions

All of these data indicate that the basaltic lava flows of the Central Atlantic magmatic province in Morocco were erupted at ca. 200 Ma and spanned the T-J boundary. Thus, it is well possible that there is a connection between this magmatic event and the T-J boundary climatic and biotic crisis, that lead to the mass-extinction.

Eastern North America

Introduction

The North American portion of the CAMP lava flows crop out in various sections in the basins of Newark, Culpeper, Hartford, Deerfield, i.e. the Newark Supergroup in New England (USA), and in the Fundy basin, all situated and in Nova Scotia (Canada). The CAMP is here constituted by rare olivine- and common quartz-normative basalts showing a great lateral extension and a maximum thickness up to 1km. The basaltic flows occur on top of continental (fluvial and lacustrine) sedimentary units of Triassic age. ⁴⁰Ar/³⁹Ar data (on plagioclase) indicate for these basaltic units an absolute age of 198-200 Ma ^{(Hames et al., 2000)}. Being this magmatic event undoubtedly close to the Triassic-Jurassic boundary, it is necessary to determine whether it straddles it or not: in this second case the CAMP couldn’t be a cause of the Tr-J mass extinction, clearly. For example, according to Whiteside et al. (2007) there are palynological, geochemical, and magnetostratigraphic evidences that the CAMP postdates the Tr-J boundary.

Magnetostratigraphy

In the Newark basin a magnetic reversal (E23r) is observed just below the oldest basalts and more or less in the same position as a palynologic turnover, interpreted as the Tr-J boundary. In Morocco, two reversal have been detected in two lava flow sequences. Two distinct correlations between the Moroccan and the Newark magnetostratigraphy have been proposed. Marzoli et al. suggest that the Tr-J boundary is located above the lower reverse polarity level which is positioned more or less at the base of the Intermediate basalt unit of Morocco. These two levels can be correlated with chron E23r of the Newark Basin, therefore the North American CAMP Basalts postdate the Tr – J boundary whereas part of the Moroccan CAMP was erupted within the Triassic. Contrarily, Whiteside et al. propose that these two levels could be earliest Jurassic intervals of reverse polarity not sampled in the Newark Basin Sequence (many more lava flows are present in the Moroccan Succession than in the Newark Basin), but observed in Early Jurassic sedimentary sequences of the Paris Basin of France. Reverse polarity intervals in America could be present within North Mountain (Fundy basin, Nova Scotia) which are poorly sampled even if previous magnetostratigraphy analysis in this sequence showed only normal polarity, or in the Scots Bay Member of the Fundy basin which have never been sampled. There is only one outcrop in the CAMP of America where reverse polarity is observable: a CAMP – related ( about 200 Ma) dike in North Carolina. Whiteside et al. suggest that reverse polarity intervals in this dike could be of post Triassic age and correlated with the same events in Morocco.

Palynological analyses

The Tr-J boundary is not officially defined, but most workers recognise it in continental strata by the last appearance index taxa such as "Ovalipollis ovalis", "Vallasporites ignatii" and "Patinasporites densus" or, in marine sections, by the first appearance of the ammonite Psiloceras planorbis. In the Newark basin the palynological turnover event (hence the Tr-J boundary mass extinction) occurs below the oldest CAMP lava flows. The same can be said for the Fundy, Hartford and Deerfield Basins. In the investigated Moroccan CAMP sections (Central High Atlas Basin), sedimentary layers sampled immediately below the oldest basaltic lava flows, apparently contain Triassic taxa (e.g., "P. densus"), and were thus defined as Triassic in age as at least the lowest lava flows ^{(Marzoli et al.,2004)}. Still, a different interpretation is suggested by Whiteside et al. (2007): the sampled sedimentary strata are quite deformed and this can mean that some sedimentary units could be lacking (eroded or structurally omitted). With respect to the Triassic pollens found in some sedimentary units above the Upper Unit basalts, they could have been reworked, so they don’t represent a completely reliable constrain.

Geochemical analyses

CAMP lava flows of North America can be geochemically separated in three units: the older ones are classified as High Titanium Quartz Normative (HTQ) basalts (TiO₂ = 1.0-1.3 wt%); these are followed by lava flows classified as Low Titanium (TiO₂ = ca. 0.8-1.3 wt%) Quartz Normative (LTQ) basalts; and then by the youngest lava flow unit classified as High Titanium (TiO₂ = 1.4-1.6 wt%) Iron Quartz Normative (HTIQ) basalts. According to Whiteside et al. (2007), geochemical analyses based upon Ti, Mg and Si contents show a certain correlation between the lower North American lava flows and the Lower Unit of the Moroccan CAMP, thus reinforcing the conclusion that the Moroccan basalts postdate the Tr-J boundary.

Therefore, according to these data, CAMP basalts shouldn’t be included among the direct causes of the Tr-J mass extinction.

References

Articles and Research Papers
*Whiteside, J.H., P.E. Olsen, D.V. Kent, S.J. Fowell, M. Et-Touhami, 2007, Synchrony between the Central Atlantic magmatic province and the Triassic-Jurassic mass-extinction event?: Palaeo, v. 244, p. 345-367.
*Marzoli, A., H. Bertrand, K.B. Knight, S. Cirilli, N. Buratti, C. Vérati, S. Nomade, P.R. Renne, N. Youbi, R. Martini, K. Allenbach, R. Neuwerth, C. Rapaille, L. Zaninetti, G. Bellieni, 2004, Synchrony of the Central Atlantic magmatic province and the Triassic-Jurassic boundary climatic and biotic crisis: Geology, v. 32-11, p. 973–976.
*Knight, K.B., Nomade, S., Renne, P.R., Marzoli, A., Betrand, H., Youbi, N., 2004. The Central Atlantic magmatic province at the Triassic–Jurassic boundary: paleomagnetic and 40Ar/30Ar evidence from Morocco for brief, episodic volcanism. Earth and Planetary Science Letters 228, 143–160.
*Hames, W.E., McHone, J.G., Ruppel, C., and Renne, P., eds., 2003, The Central Atlantic Magmatic Province: American Geophysical Union Monograph 136, 267 p.
*McHone J.G., 2000, Non-plume magmatism and rifting during the opening of the Central Atlantic Ocean: Tectonophysics, v. 316, p. 287-296.
*Marzoli, A., P.R. Renne, E.M. Piccirillo, M. Ernesto, G. Bellieni, and A. De Min, 1999, Extensive 200 million-year-old continental flood basalts of the central Atlantic magmatic province: Science, v. 284, p. 616-618.
*Wilson, M., 1997, Thermal evolution of the Central Atlantic passive margins: Continental break-up above a Mesozoic super-plume: J. Geol. Soc. London, v. 154, p. 491-495.
*Fowell, S.J., Traverse, A., 1995. Palynology and age of the upper Blomidon Formation, Fundy Basin, Nova Scotia. Review of Palaeobotany and Palynology 86 (3–4), 211–233.
*Rampino, M.R., and Stothers, R.B., 1988, Flood basalt volcanism during the past 250 million years: Science, v. 241, p. 663-668.

External links

* [http://www.auburn.edu/cosam/geo_camp The CAMP website]
* [http://www.auburn.edu/academic/science_math/res_area/geology/camp/Fig1.jpgMap of the province]