Mechanism of rift flank uplift and escarpment formation evidenced by Western Ghats, India

Abstract

The Western Ghats is one of the largest escarpments on earth, containing Reunion plume derived Deccan Traps, it is an excellent example to probe epeirogenic uplift, extension and subsidence in volcanic continental margins. The most continuous unbiased stratigraphic section of basalt down to the basement within a 1250 m drill hole of the Continental Scientific Deep Drilling Project is a valuable resource to investigate the above aspects. The flows across the entire drill core are geologically subaerial in character with basement exposed ~300 m below the mean sea level; they clearly display more evolved compositions from primary melts of mantle in terms of petrology, and only a single geomagnetic polarity transition in palaeomagnetic data. These results, combined with existing geological and geophysical data, constitute a multi-method approach that demonstrates (a) igneous underplating caused uplift prior to frequently suggested flexural isostasy (b) plume impact and eruption are near-simultaneous and extension/rifting essentially followed soon after volcanism and (c) lithosphere beneath the continental margin, while returning to normal temperatures following the Seychelles-India breakup, experienced thermal collapse and subsidence causing slumping of basalt basement below sea level.

Introduction

The Western Ghat (WG) escarpment was developed from rifting and separation of India from the Seychelles and is closely linked with the late Cretaceous (~65–66 Ma) Deccan flood basalt eruption; it demarcates the low-lying seaward coastal plains in the west from the elevated plateau to the east (Fig. 1). It is one of the largest escarpments on a volcanic continental margin in the world with over 1500 km strike length paralleling the coast and elevations ranging beyond 1 km. Therefore, this is a classic example to investigate the relationship between volcanism, plateau uplift and extension (and rifting) on volcanic continental margins. Many investigations pertain to sustained erosion and retreat of the escarpment much to the east1,2,3. These studies attribute the uplift to flexural isostasy as a result of onshore denudational unloading and offshore loading in the sedimentary basins; a few others invoked neotectonic activity for the uplift4,5. However, several lines of evidence indicate that flexural loading alone cannot be responsible for the regional uplift (~3 km onshore unroofing is required to account for sediment loading)6,7 and it requires a preexisting elevated rift flank in addition to flexural uplift. Furthermore, the uplift and elevation in a non-volcanic rift environment is not commensurate with that found in the WG and such uplift can be linked to the development of a volcanic rift margin8. McKenzie9 was the first to revive a century old idea that igneous underplating is a possible mechanism for the epeirogenic uplift in regions other than plate boundaries. That is, the rift flank topography on the west coast may have close link with the Deccan flood volcanism.

Figure 1
figure1

Topographic map of India based on Shuttle Radar Topography Mission (SRTM) data (https://earthexplorer.usgs.gov) using the 3D Analyst tool in ESRI-ArcGIS Version 10.3 Software. The Western Ghats escarpment is demarcated as a dashed white line.

There is also considerable debate on the extension/rifting and volcanism chronology. One view is that rift-margin igneous provinces form by decompression melting of a hot plume head beneath a region already undergoing extension10. Alternatively, the plume impact model11 proposes that large-scale volcanism results from melting of upwelling asthenosphere, leading to thinning of lithosphere and thereby extension and rifting. In either case, magmatic underplating is valid and may have induced rift flank uplift. Although a few isolated studies indicate magmatic underplating on the western margin of India, its linkage to uplift remained elusive. For example, a recent study of receiver function analysis12 suggests underplating in the Kutch region, but the region is much (>150 km) to the west of the escarpment in the north and it also experienced multiple tectonic episodes that may relate to different stages of the Gondwana breakup since the Triassic. The recent Continental Scientific Deep Drilling at Koyna (Fig. 1) within the WG13 gives a unique opportunity to access every successive flow of the stratigraphic section of the Deccan eruption down to the basement. In addition, geophysical investigations to bring out crustal structure in the Indian peninsular cover the WG14,15,16,17,18. Here, we assess the magmatic underplating model9 for explaining the rift-flank uplift and its mechanism along the volcanic continental margin using new and simple geological, petrological and palaeomagnetic data of the Deccan basalt down to the basement along the longest, continuous section of a drill core (1250 m; KBH-7) and by coupling the interpretations with the available geochronological, sedimentalogical, seismological and gravity results across the WG region. The WG is an ideal location for such a study using multi-method approach because a wide range of datasets are available.

Results and Description of Samples of the Scientific Deep Drilling

The KBH-7 core was drilled at an elevation of 949 m above mean sea level (MSL).The basalt sequence along the core is demarcated into 37 flows although this number varies between different authors. Individual flows (5–85 m thick), usually demarcated by red boles, generally are massive at the bottom and vesicular and/or amygdaloidal at the top. The KBH-7 core encountered a basalt-granite gneiss interface at 300 m below the present day MSL; eight other drill holes around KBH-7 also encountered basement at closely comparable depths (~250–350 m below MSL). Despite this, the drilled basalt is subaerial and does not display subaqueous signatures like pillow structures or spilitisation. In contrast, the final phase of trachyte-rhyolite-basalt volcanism in the Bombay region recorded spilitisation19. There is no stratigraphic discontinuity, like in other parts of the WG, which indicates an erosional feature and discounts a major tectonic or structural control for the formation of the escarpment. Elsewhere, normal listric faulting is common roughly parallel to the coast in the Konkan region, and the traps are downthrown to the west along the N-S normal faults20 suggesting an east-west extension. The KBH-7 did not encounter dyke intrusions.

Selected elements from geochemical data (determined by XRF and ICPMS methods) on 45 samples, taking at least one sample from each flow within the KBH-7 hole, are plotted in Fig. 2. The samples are very monotonous in composition and are Fe-rich sub-alkaline tholeiitic basalts; intermediate, silicic or alkali compositions are totally absent. The samples are low in MgO (<7.31 wt %). Correspondingly, their Mg numbers (Mg/(Mg + Fe+2) are also lower (0.52-0.36 with an exception of two samples showing values of 0.60 and 0.62) compared to the values (≥0.68) of primitive melts of the mantle. Both Cr and Ni generally behave similarly in basaltic melts and decrease along the liquid line of descent with fractionation of ferromagnesian mineral phases. Abundances of both these elements are also low in the entire KBH-7 basalt section (Cr < 300 ppm except in two samples and Ni < 112 ppm) compared to the primary melt compositions (Cr ~450–500 ppm and Ni ~250 ppm); these chemical signatures are in agreement with olivine rich (picrite) fractionation from primitive mantle melts (Fig. 3).

Figure 2
figure2

Variation of critical elemental concentrations across the drill hole KBH-7 from the surface down to the basement. The elevation (in meters) on the Y axis is with respect to MSL.

Figure 3
figure3

Zr vs Ni (left) and Cr (right) variations of KBH-7 drill core samples along with Batch melting model partial melting curves and Rayleigh fractionation modelled trends. The tie lines connecting Blue and green triangles denote picrite (ol:cpx:pl = 25:35:40) fractionation at 10% increments from 10% and 12% partial melts respectively of peridotite mantle (Zr: 8.42 ppm; Cr: 2645 ppm and Ni: 1985 ppm; values from Lyubetskaya and Korenaga47). The tie lines connecting the closed circles denote gabbro (ol:cpx:pl = 2:40:58) fractionation after 30% picrite fractionation. Tie lines connecting closed diamonds denote picrite (ol:cpx:pl = 25:35:40) fractionation (at 10% interval) from 10% partial melts. Partition coefficients for partial melting and fractionation modeling are taken from https://earthref.org/KDD/. It is seen that the KBH-7 Deccan samples are the variants between picrite-gabbro fractionated partial melts and direct picrite (with different proportions of mineral phases) fractionated partial melts.

Characteristic magnetisations were determined from azimuthally unoriented samples of each flow across KBH-7 and two other drill cores (KBH-5A and KBH-8) through detailed alternating field demagnetisations at close intervals (2.5 mT) until the stable magnetisation is achieved (details are in a manuscript under preparation). The inclination data are used here for determining the geomagnetic polarity and are plotted against MSL elevation in Fig. 4. The agreement between the three drill holes is very remarkable. The flow samples from surface down to ~640–650 m MSL show normal polarity with upward inclination (I = −50 ± 10°; n = 36) and thereafter the flow samples down to the basement show a reverse polarity with downward inclinations (I = +44 ± 14°; n = 90). These results establish unequivocally a single geomagnetic polarity transition during the eruption of the entire section of the basalt. A recent study based on mafic dykes near Bombay21 argues for four polarity transitions, but the interpretations are in conflict with the stratigraphic observations and also lack radiometric age support. The latest high-precision age data22,23,24 place the peak Deccan eruptions at about 66 Ma although a few 40Ar/39Ar ages range up to 68 Ma (see Fig. 2)25. In a comparison with geomagnetic polarity time scales, many authors26,27,28 argue that the eruptions represent 29N and 29R while some others relate them to older polarities of 30N/R or 31N/R21 (also see reference 28 for more details). In either case, the polarity data suggest that the whole eruption occurred within a short duration (<1 Ma considering 29N and 29R or <3 Ma; considering 31N and 31R). A short lower normal polarity transition is reported only from complex tectonic and structural regions.

Figure 4
figure4

Characteristic magnetization inclinations of Deccan basalt down to basement interface along three drill holes (KBH-7, KBH-8 and KBH-5A) against the mean sea level elevation. It is seen that only one geomagnetic polarity transition recorded between normal (closed symbol) and reverse (open symbols) polarity at ~640–650 m above MSL. The drill hole (KBH-5A) drilled at an elevation of 152 m MSL did not record the top normal polarity because the polarity transition is at ~640–650 m MSL elevation.

Uplifted rift-flank topography and underplating

Mantle plumes produce massive quantities of partial melt and a part of it penetrates to the surface to produce flood basalts10,29. Although estimates of volume of melt produced is not known, the entire volume of surface eruptions of the Deccan cannot account for the volume of magmas that can be generated by hot rising mantle plume. The unequivocal evidence for the evolved nature through picrite fractionation of the KBH-7 samples of the Deccan traps and similar compositions of surface samples30 and related igneous occurrences further south along the coast31, clearly indicate formation of picrite at depth in the continental crust prior to surface eruption. Such picrite, whose density is greater than the upper crust could form a layer between the crust and mantle9. A model based on petrological grounds29 also argued for magma differentiation and the formation of a picrite layer above the Moho for the Lisotho and Parana lavas and the Rooi Rand dolerites. Receiver function analysis of the teleseismic data and tomographic imaging17,18,32 and the Deep Seismic Sounding (DSS) profiling14 predicts the presence of such a horizontal layer at the crustmantle interface under the WG, with the Moho depth off-sets ranging up to 8 km. Gravity modeling coupled with inferred seismic velocity structure indicates the presence of a high density material (3.1 g/cm3) at the crust-mantle interface15. Because there is (i) no difficulty to produce uplift by magmatic intrusion at the crust-mantle interface, (ii) evidence for differentiation of olivine rich picritic magma before the magma reaching the surface and (iii) extensively widespread surface volcanism in the form of Deccan flood basalt, it is not difficult to propose uplift as a result of magma intrusion. Mantle heterogeneities modeled using viscous flow predicted dynamic surface topography of strong surface uplift along the western coastal margin of India coinciding with the timing of the Deccan eruption33. Magmatic underplating is cited to explain uplift as a result of the 260 Ma Emeishan lava eruptions in western margin of the Yangtze Craton, southwest China34. The Deccan is among the two largest flood volcanic eruptions on Earth in the last 200 Ma and the removal of melt naturally depletes the upper mantle and hence reduces its density. Presence of such a low density mantle layer (3.2 g/cm3) is inferred in the upper mantle beneath the WG region based on gravity data15. This depleted mantle also can cause uplift as can the crustal thickening by the addition of igneous rock to the crust10. Thus, the conclusion from this work presents a strong case suggesting large igneous intrusions are a major cause for epeirogenic uplift, particularly when flood basalt magmatism is present in the regions of uplift.

Flexural isostatic compensation in response to early Cenozoic erosion and deposition is evident by the drastically high rate of clastic sediment loading in the offshore basins as a result of high rate of rift-flank denudation in the WG during the Paleocene (66-56 Ma6,7). Modeled thermal histories of the apatite fission track dates also suggest higher rates of denudation at the start of the Cenozoic35. These studies also emphasise significant Neogene uplift in the WG escarpment. Mass balance studies and numerical modeling of flexural responses to onshore denudational unloading and offshore sediment loading infer that flexural isostasy alone is not adequate to explain the quantum of offshore sediment deposition6,7 and requires a pre-existing elevated rift flank. We propose here such elevated rift flank topography was formed by igneous underplating at the crust mantle interface and development of a low density depleted mantle layer on removal of melts at the time of up-rise of mantle and flood basalt eruption. An argument against such a mechanism prefers lithospheric necking for the uplift in the WG escarpment36,37. This argument assumed (i) the total uplift is due to underplating, overlooking the well recorded Neogene uplift6,7 and (ii) the uplift of rift flank topography was the result of the c. 88 Ma Madagascar-India breakup, contrary to the c. 65 Ma breakup between the Seychelles and India as suggested by many works10,30,31,38. Our present work provides clear evidence for igneous underplating based on simple petrological and geological grounds, and is supported by other published geological and geophysical results12,14,15,16,17,18,29,30.

Volcanism vs extension chronology

The results of present study also have implications for the volcanism and extension chronology in uplifted plateau regions on the volcanic continental margins. Notably, no silcic and alkaline magmatism is found across KBH-7 and the eruption of Deccan basalt is rather rapid as recorded by only a single geomagnetic polarity transition across the drill holes down to the basement; furthermore, the feeder dykes of the Deccan flows are randomly oriented39. These factors indicate that there was insufficient time for plume incubation and/or extension prior to volcanism. Intense extension and rifting followed soon after the initiation of adiabatic mantle upwelling and melting is well recorded by the preferred orientation of silicic to alkaline dykes cross-cutting the Deccan flows, slightly younger ages (~64-62 Ma) of the silicic/alkaline eruptions/intrusions in the Deccan province40,41, spilitisation in the final phase of volcanism as a result of rapid subsidence or eruption after westward down through of basalt along normal faults developed by rifting in the Bombay region, and a lack of prominent seaward dipping reflectors off the Indian west coast42. A similar chronological sequence is evident in the case of the Kerguelen plume activity also in the eastern part of India. 40Ar/39Ar ages of the igneous activity in eastern India show younger 114-105 Ma ages for alkaline magmatism compared to the slightly older 118-115 Ma peak tholeiitic flood basalt eruption43. Significant extension and crustal thinning followed, rather than preceded, the eruption of the typical continental flood basalt of the Columbia River volcanic province39,44. These interpretations are in agreement with the findings that continental uplift has often been reported prior to rifting45.

Thermal collapse and slumping down of basalt-basement interface

Finally, it is pertinent to offer an explanation for the present location of basalt-basement interface much below the MSL despite subaerial characteristics all along the Deccan section down to the basement. The heat flux associated with magma underplating decays very slowly on a time scale of the order of 50 to 100 Ma, but the heat due to upwelling of hot asthenosphere decays very fast10, particularly in case of the Reunion plume which moved away from its initial rising location. The lithosphere in western India, upon gradual cooling due to igneous underplating, became denser and the shallow basins above steadily subsided and progressively filled with shallow-water sediment derived from onshore denudation during the Palaeocene. As the temperatures returned to normal, the lithosphere experienced thermal collapse and subsidence, and thereby slumped down the basalt-basement interface far below to the level observed today in the drill cores (250–300 m below MSL). This change is also marked by the cessation of clastic sedimentary deposition in the offshore basins7. Although sea level changes could be argued as a possibility for the basalt-basement contact below MSL, the higher sea levels in the late Cretaceous (at least 200 m above the present day MSL46) do not favour the argument. Flexural isostasy appears to have become an important factor, and may have overtaken the influence of thermal subsidence, if any, by the Neogene period. The uplift appears to have resumed, as reflected by a second phase of clastic sediment deposition4,6,7, and it could be responsible for the neotectonic activity. The on-going micro-seismic activity and erosion/denudation in the WG indicate that the epeirogenic movements of flexural isostasy are still active in the Western Ghats and the denudation/erosion is likely driven mainly by uplift rather than climate.

Conclusion

This paper presents new petrological, geological and palaeomagnetic data from samples of the Deccan basalt within a continuous drill core section (s) of the Continental Scientific Deep Drilling Project in the Western Ghats, India. The data are combined with existing geological and geophysical results to explain the processes, chronological order and relationships between volcanism, uplift and extension/rifting along this volcanic continental margin. The basaltic drill core section is entirely subaerial in character and its interface with the basement is much below the mean sea level (~300 m); the section is petrologically more evolved from primary mantle melts and records only a single geomagnetic polarity transition. The main interpretations are that (a) igneous underplating was a cause of initial epeirogenic uplift in the WG, (b) extension/rifting followed shortly after volcanism and (c) thermal collapse and subsidence caused slumping down of basalt basement below sea level, while returning to normal temperatures after the Seychelles-India breakup.

References

  1. 1.

    Radhakrishna, B. P. Neogene uplift and geomorphic rejuvenation of the Indian peninsula. Curr. Sci. 64, 787–793 (1993).

  2. 2.

    Gunnell, Y. & Radhakrishna, B. P. Sahyadri, the great escarpment of the Indian subcontinent. Geol. Soc. India Memoir. 47, 717 (2001).

  3. 3.

    Kale, V. S. & Shejwalkar, N. Uplift along the western margin of the Deccan Basalt Province: is there any geomorphic evidence? J. Earth. Syst. Sci. 117, 959–97 (2008).

  4. 4.

    Valdiya, K. S. Tectonic resurgence of the Mysore plateau and surrounding regions in cratonic Southern India. Curr. Sci. 81(8), 1068–1089 (2001).

  5. 5.

    Collier, J. S. et al. Age of Seychelles-India break-up. Earth Planet. Sci. Lett. 272(1-2), 264–277, https://doi.org/10.1016/j.epsl.2008.04.045 (2008).

  6. 6.

    Campanile, D., Nambiar, C. G., Bishop, P., Widdowson, M. & Brown, R. Sedimentation record in the Konkan– Kerala basin: Implications for the evolution of the Western Ghats and the Western Indian Passive margin. Basin Res. 20(1), 3–22, https://doi.org/10.1111/j.1365-2117.2007.00341.x (2007).

  7. 7.

    Richards, F. D., Hoggard, M. J. & White, N. J. Cenozoic epeirogeny of the Indian peninsula. Geochem. Geophys. Geosyst. 17, 4920–4954, https://doi.org/10.1002/2016GC006545 (2016).

  8. 8.

    Leroy, M., Gueydan, F. & Dauteuil, O. Uplift and strength evolution of passive margins inferred from 2-D conductive modeling. Geophys. J. Int. 172, 464–476 (2008).

  9. 9.

    McKenzie, D. A possible mechanism for epeirogenic uplift. Nature 307, 616–18 (1984).

  10. 10.

    White, R. S. & McKenzie, D. P. Magmatism at rift zones: the generation of volcanic continental margins and food basalt. J. Geophys. Res. 94, 7685–7729 (1989).

  11. 11.

    Richards, M. A., Duncan, R. A. & Courtillot, V. E. Flood basalts and hot-spot tracks; plume heads and tails. Science 246, 103–107 (1989).

  12. 12.

    Rao, K. M., Ravi Kumar, M. & Rastogi, B. K. Crust beneath the northwestern Deccan Volcanic Province, India: Evidence for uplift and magmatic underplating. J. Geophys. Res. Solid Earth. 120, 3385–3405, https://doi.org/10.1002/2014JB011819 (2015).

  13. 13.

    Gupta, H. K. et al. Investigations related to scientific deep drilling to study reservoir triggered earthquakes at Koyna, India. Int. J. Earth Sci. 104, 1511–1522 (2015).

  14. 14.

    Kaila, K. L., Murty, P. R. K., Rao, V. K. & Kharetchko, G. E. Crustal structure from deep seismic soundings along the Koyna II (Kelsi-Loni) profile in the Deccan Trap area, India. Tectonophysics 73, 365–384 (1981).

  15. 15.

    Tiwari, V. M., Rao, M. B. S. V. & Mishra, D. C. Density inhomogeneities beneath Deccan Volcanic Province, India as derived from gravity data. J. Geodyn. 31, 1–17 (2001).

  16. 16.

    Rai, S. S. et al. Crustal shear velocity structure of the South Indian shield. J. Geophys. Res. 108(B2), 2088 (2003).

  17. 17.

    Rai, S. U., Rishikesh Meena, S. S., Prasad, B. N. V. & Borah, K. Moho offsets beneath the Western Ghat and the contact of Archean crusts of Dharwar Craton. Tectonophysics 672–673, 177–189 (2016).

  18. 18.

    Singh, A. et al. Crustal structure beneath India and Tibet: New constraints from inversion of receiver functions. J. Geophys. Res. Solid Earth 122, 7839–7859, https://doi.org/10.1002/2017JB013946 (2017).

  19. 19.

    Sethna, S. F. Geology of Mumbai and surrounding areas and its position in the Deccan volcanic stratigraphy, India. Jour. Geol. Soc. India. 53, 359–365 (1999).

  20. 20.

    Dessai, A. G. & Bertrand, H. The ‘Panvel Flexure’ along the western Indian continental margin: an extensional fault structure related to Deccan magmatism. Tectonophysics 241, 165–178 (1995).

  21. 21.

    Basavaiah, N., Satyanarayana, K. V. V., Deenadayalan, K. & Prasad, J. N. Does Deccan Volcanic Sequence contain more reversals than the three-Chron N–R–N flow magnetostratigraphy?—a palaeomagnetic evidence from the dyke-swarm near Mumbai. Geophys. J. Int. 213, 1503–1523 (2018).

  22. 22.

    Baksi, A. K. The Deccan Trap – Cretaceous–Paleogene boundary connection; new 40Ar/39Ar ages and critical assessment of existing argon data pertinent to this hypothesis. J. Asian Earth Sci. 84, 9–23 (2014).

  23. 23.

    Renne, P. R. et al. State shift in Deccan volcanism at the Cretaceous-Paleogene boundary, possibly induced by impact. Science 350, 76–78 (2015).

  24. 24.

    Schoene, B. et al. U-Pb geochronology of the Deccan traps and relation to the end-Cretaceous mass extinction. Science 347, 182–184 (2015).

  25. 25.

    Chenet, A. L., Quidelleur, X., Fluteau, F., Courtillot, V. & Bajpai, S. 40K-40Ar dating of the main Deccan large igneous province: Further evidence of KTB age and short duration. Earth Planet. Sci. Lett. 263, 1–15, https://doi.org/10.1016/j.epsl.2007.07.011 (2007).

  26. 26.

    Vandamme, D., Courtillot, V., Besse, J. & Montigny, R. Paleomagnetism and age determinations of the Deccan Traps (India): Results of a Nagpur-Bombay traverse and review of earlier work. Rev. Geophys. 29, 159–190, https://doi.org/10.1029/91RG00218 (1991).

  27. 27.

    Jay, A. E., Niocaill, C. M., Widdowson, M., Self, S. & Turner, W. New palaeomagnetic data from the Mahabaleshwar Plateau, Deccan Flood Basalt Province, India: implications for the volcanostratigraphic architecture of continental flood basalt provinces. J. Geol. Soc. London. 166, 13–24, https://doi.org/10.1144/0016-76492007-150 (2009).

  28. 28.

    Chenet, A. L. et al. Determination of rapid Deccan eruptions across the Cretaceous–Tertiary boundary using paleomagnetic secular variation: 2. Constraints from analysis of eight new sections and synthesis for a 3500-m-thick composite section. J. Geophys. Res. 114, B06103, https://doi.org/10.1029/2008JB005644 (2009).

  29. 29.

    Cox, K. G. A Model for Flood Basalt Volcanism. J. Petrol. 21, 629–650 (1980).

  30. 30.

    Mahoney, J. J. Deccan Traps. In Continental Flood Basalts (ed.) Macdougall, J. D. 151–194. (Dordrecht: Kluwer Acad, 1988).

  31. 31.

    Radhakrishna, T. & Joseph, M. Geochemistry and paleomagnetism of late Cretaceous mafic dikes in Kerala, southwest coast of India in relation to large igneous provinces and mantle plumes in the Indian Ocean region. Geol. Soc. Am. Bull. 124(1/2), 240–255, https://doi.org/10.1130/b30288.1. (2012).

  32. 32.

    Gupta., S. et al. The nature of the crust in southern India: implications for Precambrian crustal evolution. Geophy. Res. Letts. 30, 1419–1423 (2003).

  33. 33.

    Glišovi, P. & Forte, A. M. On the deep-mantle origin of the Deccan Traps. Science 355, 613–616 (2017).

  34. 34.

    Xu, Y. G. & He. Thick, high-velocity crust in the Emeishan large igneous province, SW China: Evidence for crustal growth by magmatic underplating or intraplating, in Foulger, G. R. and Jurdy, D. M., eds, Plates, plumes, and planetary processes: Geol. Soc. Spec. Pap. 430 (2007).

  35. 35.

    Gunnell, Y., Gallagher, K., Carter, A., Widdowson, M. & Hurford, A. J. Denudation history of the continental margin of western peninsular India since the early Mesozoic – reconciling apatite fission track data with geomorphology. Earth Planet. Sci. Lett. 2, 187–201 (2003).

  36. 36.

    Chand, S. & Subrahmanyam, C. Rifting between India and Madagascar – mechanism and isostasy. Earth Planet. Sci. Lett. 210, 317–332 (2003).

  37. 37.

    Sheena, D. V., Radhakrishna, M., Chand, S. & Subrahmanyam, C. Gravity anomalies, crustal structure and rift tectonics at the Konkan and Kerala basins, western continental margin of India. J. Earth Syst. Sci. 121, 813–822 (2012).

  38. 38.

    Storey, M. et al. Timing of hotspot related volcanism and the break-up of Madagascar and India. Science 267, 852–855, https://doi.org/10.1126/science.267.5199.852 (1995).

  39. 39.

    Hooper, P. R. The timing of crustal extension and the eruption of continental flood basalts. Nature 345, 246–249, https://doi.org/10.1038/345246-0 (1990).

  40. 40.

    Sheth, H. C., Pande, K. & Bhutani, R. 40Ar- 39Ar ages of Bombay trachytes: Evidence for a Palaeocene phase of Deccan volcanism. Geophys. Res. Lett. 28, 3513–3516, https://doi.org/10.1029/2001GL012921 (2001).

  41. 41.

    Hooper, P., Widdowson, M. & Kelley, S. Tectonic setting and timing of the final Deccan flood basalt eruptions. Geology 38, 839–842 (2010).

  42. 42.

    Todal, A. & Eldholm, O. Continental margin of western India and Deccan large igneous province. Mar. Geophys Res. 20, 273–291 (1998).

  43. 43.

    Radhakrishna, T., Soumya, G. S. & Satyanarayana, K. V. V. Palaeomagnetism of the Cretaceous Lamproites from Gondwana basin of the Damodar Valley in India and migration of the Kerguelen plume in the Southeast Indian Ocean. J. Geodyn. 109, 1–9 (2017).

  44. 44.

    Colgan, J. P., Dumitru, T. A., McWilliams, M. & Miller, E. L. Timing of Cenozoic volcanism and Basin and Range extension in southwestern Nevada: New constraints from the northern Pine Forest Range. Geol. Soc. Am. Bull. 118, 126–139 (2006).

  45. 45.

    Le Bas, M. J. Per-alkaline volcanism, crustal swelling, and rifting. Nature Phys. Sci. 230, 85–87 (1971).

  46. 46.

    Haq, B. U. Cretaceous eustasy revisited. Glob Planet Change. 113, 44–58 (2014).

  47. 47.

    Lyubetskaya, T. & Korenaga, J. Chemical composition of Earth’s primitive mantle and its variance: 1. Method and results. J. Geophys. Res. 112, B03211, https://doi.org/10.1029/2005JB004223 (2007).

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Acknowledgements

Dr. Harsh Gupta, the President of the Geological Society of India has prompted and motivated us to initiate this work. Dr. B.K. Bansal (Advisor, Ministry of Earth Sciences (MoES), Government of India), Dr. V.M. Tiwari Director, CSIR-NGRI and Dr. P.C. Rao, Director, NCESS are instrumental in making us to write this ms. Sri S. Rajappan extended help in preparing the SRTM topographic map. Samples for this study were obtained from the Borehole Geophysics Research Laboratory (BHRL), Karad. The ms is benefitted from the comments/corrections by an anonymous reviewer. The work is supported by grants from the MoES (MoES/P.O. (Seismo)/(195)/2013) and CSIR Emeritus Scientist scheme 21(1041)/17/EMR-II.

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R.T. designed the research, did data processing and wrote the manuscript; A.R.M. and V.M. participated in sample collection, did the sample processing and palaeomagnetic analysis; S.G.S. participated in palaeomagnetic analysis and in data analysis; P.P.K. participated in sample collection and did sample preparation for geochemical analysis; all authors edited the ms.

Correspondence to Radhakrishna T..

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