Letter | Published:

Cryptic striations in the upper mantle revealed by hafnium isotopes in southeast Indian ridge basalts

Nature volume 440, pages 199202 (09 March 2006) | Download Citation



The Earth's mantle is isotopically heterogeneous on length scales ranging from centimetres to more than 104 kilometres1,2. This heterogeneity originates from partial melt extraction and plate tectonic recycling, whereas stirring during mantle convection tends to reduce it. Here we show that mid-ocean ridge basalts from 2,000 km along the southeast Indian ridge (SEIR) display a bimodal hafnium isotopic distribution. This bimodality reveals the presence of ancient compositional striations (streaks) in the Indian Ocean upper mantle. The number density of the streaks is described by a Poisson distribution, with an average thickness of 40 km. Such a distribution is anticipated for a well-stirred upper mantle, in which heterogeneity is continually introduced by plate tectonic recycling, and redistributed by viscous stretching and convective refolding.


The SEIR stretches from the Rodrigues Triple Junction (25.6° S, 70.1° E) to the Macquarie Triple Junction (62° S, 151° E). Between 76°–78° E it crosses the Amsterdam–St Paul (ASP) plateau, a pronounced bathymetric swell associated with relatively hot mantle upwelling beneath the Amsterdam and St Paul islands, while between 120° E and 128° E it crosses the Australian–Antarctic discordance (AAD), a region of deep bathymetry (> 4,000 m) associated with relatively cold mantle and low melt production3. Notably, over a distance of 2,500 km, between 86° E and 120° E, there is a regular eastward decrease in axial depth from 2,300 to 5,000 m, and a morphological transition from axial high to axial valley due to decreasing melt production rate and crustal thickness. This depth gradient occurs at an intermediate and uniform spreading rate (70–75 mm yr-1 full rate) and in the absence of large transform offsets and nearby mantle hotspots. The range in axial depth and ridge morphology is similar to the global range for spreading ridges away from hotspots, making the SEIR a regional-scale analogue of the 50,000-km-long global ocean ridge system. Previous work has established that the He, Pb, Sr and Nd isotope variations along the SEIR are primarily controlled by variation in the depth of melting of isotopically heterogeneous mantle4,5,6,7. Also, all SEIR lavas west of the AAD are true ‘Indian-type’ on the basis of their elevated 208Pb/206Pb ratios6.

New Hf isotope results have been obtained for 48 SEIR basalts previously analysed for He-Ne-Ar and Pb-Nd-Sr isotope compositions4,5,6,7 (see Supplementary Table 1). All samples are fresh mid-ocean ridge basalt (MORB) glasses that were microscopically hand-picked to be free of surface alteration. Between 300 and 600 mg of this glass was digested and the Hf separated using ultrapure reagents and following established techniques8. The new results show a +5.5 to +17.8 range in ɛHf (defined in Fig. 1). The extreme ɛHf values for the data presented here occur on the ASP plateau (+ 5.5) and in the westernmost AAD (+ 17.8), and are within the range of values measured previously in those areas9,10,11,12. Broadly speaking, Hf and Nd isotopes in our sample suite show the positive correlation typical of most oceanic basalts13. However, in detail the Hf isotope variations are not simply related to axial depth, ridge segmentation, MORB type or Sr-Nd-Pb-He isotopic variations.

Figure 1: Along-axis variations in ɛHf for basalt glasses from the SEIR.
Figure 1

ɛHf = (176Hf/177Hfmeasured/176Hf/177HfBSE - 1) × 104, where BSE is the bulk silicate Earth reference value of 176Hf/177HfBSE = 0.282772 (ref. 16). New data from this study are shown as solid circles; other data are from refs 9–12. The dashed box outlines the area shown in Fig. 2a.

The striking attribute of this new data set, previously unobserved in MORBs, is the Hf isotopic bimodality for lavas erupted between 88° E and 110° E (Fig. 2). Over this 2,000-km length of actively spreading ridge the two groupings show a ‘gap’ of about one epsilon unit (ɛHf = +9.5 to +11.5 and +12.5 to +14.6, respectively). This ɛHf gap is significantly larger than the analytical uncertainty (2σ external precision is 0.3 epsilon units). Because our sample suite has a strong spatial resolution, the results suggest the presence of striations (streaks) in the upper mantle beneath the SEIR. The ɛHf bimodality is not observed in other geochemical parameters, including Nd isotope composition, indicating that the streaks carry a cryptic memory of ancient chemical fractionation that is now only apparent in the time-integrated Lu/Hf ratio. Because ɛNd along this section of the SEIR is not bimodal, Lu–Hf and Sm–Nd fractionation must have been decoupled at some point in the evolutionary history of the underlying upper mantle.

Figure 2: The Hf isotope bimodality.
Figure 2

a, Detailed view of the bimodal ɛHf region between 88° E and 110° E. The data clearly show two groupings separated by more than one epsilon unit, with high and low values delineated by the alternating stripes numbered 1 to 18 from west to east. The solid curve is a smoothed running mean using a gaussian spatial filter that has a standard deviation of 150 km. b, The histogram (n = number of samples) shows the deviations (Δ) from the running mean in a. Nd isotopes have been treated similarly to the Hf isotope data and are shown for comparison. Student's t-test indicates that the probability of the Hf isotopes being drawn from a single population is 0.1%.

There are several possible origins for the bimodality in Hf isotopes and decoupling of Nd and Hf isotopes, most of which involve mixing with recycled mantle components (Fig. 3). One possibility is a remnant of primordial heterogeneity, perhaps resulting from the presence of a deep magma ocean. Given the efficiency of mantle convection in eradicating such remnants14, this explanation seems unlikely, but it cannot be completely ruled out15. A second possibility is ancient melting that involved a variable amount of garnet restite, such as during komatiite formation16. The observed north–south ɛHf gradient in depleted Atlantic MORB and its relation to distance from the continents can be accounted for in this way17,18.

Figure 3: Global ɛHf–ɛNd correlation for 2,100 oceanic basalts.
Figure 3

Data are from the literature and from J.B.-T.'s unpublished database. The dashed line is the linear regression for all data (ɛHf = 1.3ɛNd + 3.3; R2 = 0.70). The bimodal distribution of SEIR basalts is illustrated by the black circles; basalts from the Amsterdam and St Paul islands11, shown by the triangles, display a similar bimodality in ɛHf. Examples of potential recycled endmembers that may be involved in mantle mixing are included for comparison (AG = Australian granulite, PS = pelagic sediment, SAG = South African granulite; for example, see ref. 23).

A third possibility involves mixing of different proportions of tectonically subducted components (altered oceanic crust/lithosphere, pelagic sediment and fluid-modified mantle wedge from subduction zones) with mantle peridotite. Fluid-modified, melt-depleted mantle wedge beneath subduction zones may display ɛHf lying above the Hf–Nd mantle array19. Variability in the mixing proportion of recycled sediment would produce a covariation in ɛNd–ɛHf, and is therefore unlikely, by itself, to account for the observed Hf isotope bimodality. However, variability in the proportion of pelagic sediment plus hydrothermally altered crust might produce the bimodality, if Hf/Nd ratios in the recycled material range to both higher and lower values than Hf/Nd in the ambient upper mantle (in which case mixing curves in Hf–Nd isotopic space would diverge and could be strongly hyperbolic).

A fourth possibility is a difference in the mineralogic/lithologic make-up of the mantle source. For example, clinopyroxene in the residue of mantle melting can develop radiogenic ɛHf at relatively invariant ɛNd over 108-year timescales, owing to its depletion in high-field-strength elements20. However, there is no evidence for covariation between Hf isotopes in SEIR basalts and potential indicators of modal clinopyroxene abundance or mantle source fertility, such as Sc/Nb or CaO/Al2O3 ratios. A fifth possibility is recycling of mid-crustal amphibolite or high-temperature granulite facies rocks in which rutile and iron–titanium oxides control Lu/Hf and the extent of Hf depletion, as evidenced by significant Lu/Hf–Sm/Nd decoupling in crustal xenoliths from southern African kimberlites21. Lastly, garnet in some cratonic peridotites from South African kimberlites shows ɛHf = +200 to +400, while ɛNd ranges only between 0 and +15 (ref. 22). The significant potential for Hf–Nd isotopic decoupling by recycling of continental lithospheric mantle may account for the isotopic variations observed along the southwest Indian ridge23.

Regardless of their exact origin, the different mantle source regions beneath the SEIR sampled by the MORB Hf isotope bimodality have primarily witnessed a history of coupled Lu/Hf–Sm/Nd fractionation similar to most of the oceanic mantle, because the bimodal populations lie close to the modern ɛHf–ɛNd array for oceanic basalts and as a group adhere to the overall trend in this diagram (Fig. 3).

Spatially, the streaks defined by the Hf isotope bimodality are well described as a Poisson distribution, in which the number of Hf isotope ‘toggles’ between the two groupings is proportional to the length of ridge sampled (Fig. 4a). A Poisson distribution describes the total number of independent events that occur within a specified interval for a fixed mean value of the ‘arrival rate’; it is characterized by a number of events proportional to the length of the observation span (for example, as exemplified by radioactivity). The number of Hf isotope ‘toggles’ in SEIR basalts closely follows this prediction over a ridge length of >2,000 km, as expected for a Poisson distribution of cryptic streaks in the underlying mantle. Moreover, when the number of striation boundaries follows a Poisson distribution, the intervals between boundaries (that is, the striation thicknesses) follow an exponential distribution, as observed in the current data set (Fig. 4b). The Hf isotope ‘toggles’ are not as well-discerned outside the 88° E to 110° E section of the SEIR, and seem to be absent where the geodynamic setting is more complex, such as on top of the ASP plateau and within the AAD. Given the sampling density along the SEIR, the mean thickness of the striations in the underlying mantle appears to be 40 km (Fig. 4a inset).

Figure 4: Poisson character of upper mantle streaks beneath the SEIR.
Figure 4

a, Cumulative number of Hf isotopic striations versus distance (in kilometres) along the SEIR. The line shown is a linear regression (y = 0.0107x + 0.487, R2 = 0.992, n = 29; 1σ uncertainties on the slope and intercept are 0.00099 and 0.988, respectively). The mean thickness of the striations, based on the slope of this diagram, would be 93 km (± 9 km, 1σ). The inset illustrates how the inferred mean thickness of the striations is affected by sampling density. A large population with a uniform density for the probability of a transition between two different mantle ‘flavours’ has been approximated by 1,000 points spread randomly along a line. The distance between two consecutive points represents the thickness of an individual striation. This model has an exponential distribution of striation thicknesses, consistent with the observed relationship between cumulative number of transitions and distance. As expected, the proportion of striations recovered during sampling increases as the sampling density (that is, number of samples per striation) increases. Because the sampling density along the SEIR has 1.6 samples per striation, about 40% of the striations present in the underlying mantle have been sampled, indicating that the true mean thickness of the striations is 40 km. b, Probability diagram of the width (thickness) of the Hf isotopic striations. The x axis shows the percentage of striation widths (normalized to a normal probability distribution) whose value is less than the respective value of the y-axis data point. The solid curve is an exponential fit (y = 89.71exp[0.476x], R2 = 0.971) and the dashed line is a linear fit (y = 100.4 + 48.97x, R2 = 0.86). This good exponential relationship is consistent with a Poisson distribution for the number density of upper mantle striations.

Let us define a geochemical heterogeneity as a point on the boundary between two types of mantle, for example, a mantle residue of partial melting versus recycled crust or lithosphere. A Poisson distribution of geochemical heterogeneities should be anticipated as the natural consequence of a well-stirred upper mantle in which heterogeneities are continually created by tectonic recycling and redistributed by convective stretching and refolding. The mean striation thickness is therefore a useful parameter for quantifying mantle strain rate24. Strain rates associated with mantle convection are of the order of 10-15 s-1 (ref. 25). After 40 million years (Myr), recycled material would have been stretched and reduced to about 50% of its original thickness via shear strain, and after 300 Myr to about 10%. (Corresponding timescales for stretching by normal strain are shorter, 25 and 80 Myr, respectively; Supplementary Fig. 1.)

The timescale of 300 Myr is similar to that inferred from comparative U–Pb, Sm–Nd and Rb–Sr isotope systematics of enriched and depleted MORB worldwide. This timescale potentially represents a convective cycling time within the mantle, either for oceanic lithosphere and metasomatized mantle subducted beneath island arcs or for continental lithosphere delaminated during rifting, to the eventual resampling by partial melting beneath mid-ocean ridges26,27,28. Notably, the Pb, Nd, Sr and Hf isotopes in SEIR basalts are correlated with their respective parent/daughter ratios, and each of these correlations also imply ‘ages’ of 200–400 Myr (ref. 6 and Supplementary Fig. 2). However, these age estimates have large uncertainties, and probably represent minimum values because the slopes of the correlations could also have been affected by varying U/Pb, Sm/Nd, Rb/Sr and Lu/Hf ratios during melting.

The narrow range of ɛHf of <5 units in the bimodal region makes it currently impossible to discriminate between the possible origins of the streaks, because diagnostic geochemical signatures associated with the small extent of Lu/Hf–Sm/Nd decoupling are extremely weak in this sample suite. Nevertheless, the fact that the Amsterdam and St Paul islands display the same Hf isotope bimodality11 as the SEIR MORBs studied here (Fig. 3) suggests a significant role for upwelling plumes in convective dispersion and refolding of such mantle streaks, and is further evidence that regions of the upper mantle far from any active hotspot influence still retain a record of past pollution by mantle plumes29.

The isotopic compositions of mantle-derived materials provide constraints on crust/mantle differentiation and planetary evolution, while their spatial distribution is fundamentally linked to mantle dynamics. The Hf isotope bimodality along the SEIR represents the first observational evidence that a Poisson distribution of heterogeneous streaks characterizes large sections of the upper mantle. We speculate that this distribution is more easily recognized along the SEIR than along other sections of the mid-ocean ridge system, because the SEIR is uncomplicated by the effects of nearby mantle hotspots, continental land masses, or large fracture zone offsets. Striation thickness distributions in realistic, time-periodic flows of viscous fluids, such as those appropriately describing aspects of the Earth's mantle, are extremely difficult to model numerically given the computational state-of-the-art. However, striation thickness distributions can be accurately predicted from a knowledge of the stretching values30. A Poisson distribution of mantle heterogeneities, and the associated exponential distribution of striation thicknesses, is a fundamental mantle property that should be taken into account in forthcoming models of mantle convection and rheology.


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D.W.G. thanks A. Bouvier, A. Agranier, P. Beck, F. Moynier, K. Koga and E. Koga for their help and hospitality during two extended visits to Lyon. We thank P. Telouk for his help with the P54 mass spectrometer. D. Christie, B. Hanan, K. Johnson, J. Mahoney and D. Pyle provided help on many aspects of SEIR geochemistry. N. Pisias provided insight into some of the nuances of statistical distributions. D.W.G., C.J.R. and K.H.R. were supported by the Marine Geology division of the NSF, and J.B.-T. and F.A. by the French Institut National des Sciences de l'Univers. Author Contributions D.W.G. and J.B.-T. performed the Hf isotope measurements. All authors contributed to data analysis.

Author information


  1. College of Oceanic and Atmospheric Sciences, Oregon State University, Corvallis, Oregon 97331, USA

    • D. W. Graham
    •  & C. J. Russo
  2. Laboratoire des Sciences de la Terre, Ecole Normale Superieure, 69364 Lyon, France

    • J. Blichert-Toft
    •  & F. Albarède
  3. SOEST, University of Hawaii, Honolulu, Hawaii 96822, USA

    • K. H. Rubin


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Correspondence to D. W. Graham.

Supplementary information

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  1. 1.

    Supplementary Table 1

    Hf isotope and sample location data for Southeast Indian Ridge basalts.

  2. 2.

    Supplementary Figure 1

    Two diagrams illustrating the stretching of mantle bands by shear strain (A) and normal strain (B), respectively.

  3. 3.

    Supplementary Figure 2

    Lu-Hf isochron diagram for Southeast Indian Ridge basalts.

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    Text to accompany Supplementary Figures 1 and 2.

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