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Slow slip along the Hikurangi margin linked to fluid-rich sediments trailing subducting seamounts

Nature Geoscience volume 16, pages 505–512 (2023)Cite this article

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Abstract

Large seamounts and basement relief cause permanent deformation when they collide with the overriding plate at subduction zones. The resulting structural and compositional heterogeneities have been implicated as controlling factors in megathrust slip behaviour. Subducting seamounts may temporarily lock plates, favouring subsequent large earthquakes. Alternatively, seamounts may redistribute stress, reducing seismic slip. Here we present three-dimensional seismic data from the seamount-studded subducting Hikurangi Plateau along New Zealand’s North Island. We find that one well-imaged seamount, the Pāpaku Seamount, locally uplifts the overriding plate and leaves a tube-shaped lens of sediment trailing in its wake. Anomalously low seismic velocities within and below the Pāpaku lens and along the megathrust fault are consistent with the presence of unconsolidated, overpressured fluid-rich sediments. Similar observations from an older sediment lens, which corresponds to the location of a 2014 slow-slip rupture event, suggest that such overpressures can persist along the megathrust due to delayed drainage out of the subducting plate. The collocation of the 2014 slow-slip earthquake with this sediment lens suggests that these fluid-rich regions define zones that enable slow slip. We hypothesize that sediment lenses left behind by subducting seamounts can create low-effective-stress patches within transitionally stable marine sediment along the megathrust that are conducive to slow slip.

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Fig. 1: Bathymetric map of the Hikurangi margin.
Fig. 2: Seismic profiles across the Hikurangi margin.
Fig. 3: Perspective view of seismic volume looking southwest.
Fig. 4: Perspective views of the 3D volume looking northeast.
Fig. 5: Perspective view of the northern Hikurangi margin looking west showing seamount collisions.

Data availability

Raw seismic reflection data are available at https://doi.org/10.1594/IEDA/324554 (ref. 49). The processed 3D PSDM data used in interpretation are available at https://doi.org/10.26022/IEDA/331022 (ref. 50). The seismic velocity model produced from 3D full-waveform inversion and used in the interpretation are available at https://doi.org/10.26022/IEDA/331023 (ref. 51). Ocean-bottom seismometer data are available via https://www.jamstec.go.jp/rimg/e/. Bathymetry data are available via https://niwa.co.nz/oceans/tools-and-resources. All data from MGL1801 (Cruise DOI: 10.7284/907876) are available at https://www.marine-geo.org/tools/search/entry.php?id=MGL1801.

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Acknowledgements

We thank the captains, crew and onboard science parties of the RV Tangaroa and the RV Marcus G. Langseth for their contribution to the data acquisition. We thank Paradigm Geophysical for providing software. We thank NIWA for providing bathymetry data. The academic NZ3D project was financially supported by US NSF (award #s 1559298 (N.L.B., S.H. and A.C.G.), 1901645 (N.L.B. and S.H.), 1559008 (G.F.M. and H.L.T.), 2023186 (G.F.M. and H.L.T.), 1558574 (H.J.T.) and 1558440 (J.H.E.)), NERC NE/M021203/1 (R.E.B., R.D. and L.F.), JAMSTEC (R.A. and S.K.), NZ MBIE and GNS Science (D.H.N.B., S.A.H., D.B., R.K., V.S. and B.F.).

Author information

Authors and Affiliations

  1. Institute for Geophysics, Jackson School of Geosciences, University of Texas at Austin, Austin, TX, USA

    Nathan L. Bangs, Shuoshuo Han & Andrew C. Gase

  2. Department of Earth, Environmental and Planetary Sciences, Rice University, Houston, TX, USA

    Julia K. Morgan

  3. Department of Earth Science and Engineering, Imperial College, London, UK

    Rebecca E. Bell, Richard Davy & Laura Frahm

  4. Japan Agency for Marine–Earth Science and Technology, Yokohama, Japan

    Ryuta Arai & Shuichi Kodaira

  5. School of Earth and Space Sciences, University of Science and Technology of China, Hefei, China

    Xinming Wu

  6. Department of Earth Sciences, University of Hawai’i at Manoa, Honolulu, HI, USA

    Hannah L. Tilley & Gregory F. Moore

  7. Marinespace, Southampton, UK

    Hannah L. Tilley

  8. GNS Science, Lower Hutt, New Zealand

    Daniel H. N. Barker, Stuart A. Henrys, Dan Bassett, Richard Kellett, Valerie Stucker & Bill Fry

  9. Department of Earth and Planetary Sciences, University of California, Santa Cruz, CA, USA

    Joel H. Edwards

  10. Zanskar Geothermal & Minerals, Inc, Salt Lake City, UT, USA

    Joel H. Edwards

  11. Department of Earth and Space Science, University of Washington, Seattle, WA, USA

    Harold J. Tobin

  12. School of Geography, Earth and Environmental Science, University of Birmingham, Birmingham, UK

    Tim J. Reston

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Contributions

N.L.B., R.E.B., S.K., R.A. and S.A.H., designed the experiment. N.L.B., S.H. H.L.T., D.H.N.B., J.H.E, H.J.T, T.J.R. D.B. R.K., V.S. and B.F. helped with data acquisition at sea on the RV Lanseth or RV Tangaroa. N.L.B. and S.H. directed CGG in data processing. N.L.B., J.K.M., S.H., A.C.G. and X.W. conducted the data interpretation. R.E.B., R.D. and L.F. conducted initial full-waveform inversions. All authors contributed to the writing of this manuscript.

Corresponding author

Correspondence to Nathan L. Bangs.

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Nature Geoscience thanks Jacob Geersen, Jean-yves Collot and the other, anonymous, reviewer(s) for their contribution to the peer review of this work. Primary Handling Editor: Louise Hawkins, in collaboration with the Nature Geoscience team.

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Extended data

Extended Data Fig. 1 Inline 774 from the NZ3D seismic data volume with and without the velocity model.

Top image is the seismic profile. This is the same line as shown in Fig. 2, but without interpretation. Bottom section has an overlay of the velocity model. See Fig. 1 for location.

Extended Data Fig. 2 Inline 188 from the NZ3D seismic data volume with and without the velocity model.

Top image is the seismic profile. This is the same line as shown in Fig. 2, but without interpretation. Bottom section has an overlay of the velocity model. See Fig. 1 for location.

Extended Data Fig. 3 Map showing locations of features discussed in the text.

Map directly overlaps with Fig. 1 and shows the seamounts and sediment lenses in NZ3D survey area (black rectangle), and slip during the 2014 slow slip event21. Barbed black line marks the deformation front. The NZ3D survey is 15 × 65 km2. Red dashed lines (with green shading) are seamount locations imaged within the 3D volume. Dark blue shading shows the outline of an inferred seamount from Barker et al.25) based on a two-dimensional seismic profile and magnetic anomalies. Cyan shading shows the position of a sediment lens in the wake of the Pāpaku seamount and beneath the Pāpaku fault, and second sediment lens believed to have formed from an older, subducted seamount. Slip contours are in mm.

Extended Data Fig. 4 Three-dimensional perspective view showing the sediment lens geometry.

This view looks north and shows the seismic data volume with the sediment lens (light shading) updip from the Pāpaku seamount. The Pāpaku sediment lens formed in the wake of the subducting Pāpaku seamount. The yellow surface is the Pāpaku fault, which forms a lateral ramp that intersects the décollement in an arcuate pattern. It extends farthest downdip above the Pāpaku seamount peak. The sediment lens beneath the Pāpaku fault fills in the space updip from the Pāpaku seamount. The peak of the Pāpaku seamount lies directly updip from the thickest section of the sediment lens, which thins to the SW updip of the flank of the Pāpaku seamount. A second sediment lens lies beneath Tuaheni ridge and is believed to have formed from an older subducted seamount.

Extended Data Fig. 5 Perspective view showing the sediment lens beneath the Pāpaku fault and underlying basement seismic velocities.

Light shading shows the geometry of the sediment lens beneath the Pāpaku fault. The colored surface lies 500 m below the top of the subducting basement (red line) and shows the average velocity within the uppermost 500 m of subducting basement. Basement velocities are consistently lower beneath the sediment lens associated with the Pāpaku seamount than regions outside of the influence of the sediment lens to the southwest. This correlation suggests that the sediment lens inhibits drainage from beneath it.

Extended Data Fig. 6 Inline 480 from the NZ3D seismic data volume with and without the velocity model.

Top image is the seismic profile. Bottom section has an overlay of the velocity model. Inline 480 is located mid-way between Inlines 188 and 774, which are located in Fig. 1. This line lies ~ 350 m south of the IODP Expedition 372/375 drilling transect.

Extended Data Fig. 7

Full-waveform inversion models of streamer and OBS records. Surface streamer shot record (top) and a portion of an OBS shot record (bottom) with an FWI model from inversion up to 7 Hz superimposed on top. The positive lobe of the signal is shaded in black and the negative left unshaded to show where fit is good (blue showing) and poor (red showing). Models of both the reflections in the shot records and refractions in the OBS records fit the data well, and were further improved in subsequent inversions.

Extended Data Fig. 8 Common image gathers (CIG) across Inline 500 showing the flattening of deep events following depth migration using the FWI/tomographic inversion model.

Gathers are flattened across the full range of offsets within depths equivalent to regions interpreted in Figs. 3, 4, Supplementary Figs. 4 & 5. These flattened gathers help validate the velocity model.

Extended Data Fig. 9 OBS20 geophone record showing first arrivals and the corresponding model result.

Shown is one record from one of 97 OBS used in the FWI and tomographic inversion. a) OBS20 record with first arrivals picked (blue line) to compare with synthetic model. b) Synthetic model produced from FWI and tomographic inversion of OBS 20. First arrival picked (red line) to compare with data. c) Comparison of first arrivals from OBS 20 and synthetic seismogram derived from FWI and tomographic inversion by CGG Services (Singapore) showing excellent agreement at all offset ranges out to ~25 km. FWI was limited to 25 km offsets due to previous shot noise and weak signals at higher offsets. ε and δ are Thomsen anisotropy parameters52. See Arai et al.30 for location.

Extended Data Fig. 10 Comparison of the initial and the final images for Inline 500.

The initial (top) and the final (bottom) images for Inline 500 produced with initial and final velocity models to show improved continuity of major reflections, reduced interference from reflections crosscutting primary reflections, higher reflection amplitudes, and more geologically realistic structures.

Supplementary information

Supplementary Information

Supplementary Figs. 1–13, Discussions and references.

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Bangs, N.L., Morgan, J.K., Bell, R.E. et al. Slow slip along the Hikurangi margin linked to fluid-rich sediments trailing subducting seamounts. Nat. Geosci. 16, 505–512 (2023). https://doi.org/10.1038/s41561-023-01186-3

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