Pn tomographic velocity and anisotropy beneath the Tibetan Plateau and the adjacent regions
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2011
Received: 9 April 2011
Accepted: 21 July 2011
Published: 14 February 2012
We present a tomographic velocity and anisotropy model of the uppermost mantle beneath the Tibetan Plateau and the adjacent regions. The investigation analyzed 105,385 Pn phase readings from the International Seismological Centre (ISC) and the China Earthquake Data Center. The average Pn velocity under the study area is approximately 8.15 km/s, with velocity perturbations up to 3–4%. We find high Pn velocities under the Indian Plate and in the Tarim and Sichuan basins, low Pn velocities under the Hindu Kush and in Myanmar and the adjacent region, and especially low Pn velocities under the area north of the Indus-Yarlung Zangbo suture. The high Pn velocity anomalies of the Indian Plate are discontinuous at the collision region in the east-west direction, indicating that the Indian Plate probably subducts in a piecewise manner. Distributions of Pn velocities are used to validate mechanisms for the subduction of the Indian Plate presented in previous studies. In addition, Pn anisotropy is obtained simultaneously with Pn velocity. At plate collision zones, the fast Pn anisotropy direction is parallel to the direction of the collision edge. We validate the existence of Pn anisotropy under these regions and discuss the relationship of anisotropy with tectonic structure and plate movement.
Key wordsPn velocity anisotropy Indian Plate Tibetan Plateau
In the uppermost mantle, changes in composition, temperature, pressure and water volatile content contribute to Pn velocity variations. The preferred alignment of olivine crystals, caused by the creeping of material in the uppermost mantle, is believed to contribute to Pn velocity anisotropy (Ribe, 1992). Thus, Pn velocity variations and anisotropy provide constraints on the processes of continental deformation and differentiation.
This region has been studied in the past by various authors (e.g., Kind et al., 2002; Liang et al., 2004, 2006; Sun and Toksöz, 2006; Pei et al., 2007; Phillips et al., 2007; Zheng et al., 2007; Sun et al., 2008). In these studies, high Pn velocities have been discovered beneath the Indian Plate and low velocities have been found in the eastern India and Myanmar regions. Pn anisotropy models have also been developed by previous studies. However, advances in tomography technology have led to a denser seismic ray path coverage than those in earlier studies. Here, we present improved Pn velocity and anisotropy tomographic models of the uppermost mantle beneath the Tibetan Plateau and the adjacent regions using both seismic data from the Chinese Earthquake Network catalogs and data from the ISC catalogs. This new dataset contains Pn arrival readings from stations in both India and China, thus providing tighter constraints on the velocity structure near the India-China border. These high-resolution data are very useful for the investigation of the complex tectonics of this region. The distributions of Pn velocities and anisotropy provide some hypotheses on the subduction mechanisms of the Indian Plate.
2. Data and Method
For the inversion, we used Pn data for which the epicenter distance range was between 2° and 12°. We chose the lower limit of 2° to remove the Pg phases and the upper limit of 12° to include only the observations along the linear portion of the travel time curve, as well as to avoid arrivals from the deeper part of the upper mantle. Within this distance range, the Pn phases are the first arrivals. The initial models were obtained by a linear fit to the traveltime-distance curve. The traveltime residuals to the fitted line used in this paper are limited to a range of ±6s. Using this methodology, 105,385 Pn rays were obtained.
3. Checkerboard Test
4. Results and Discussion
The Indian Plate, which is subducting under Myanmar and the adjacent region from the southwest, displays obvious low Pn velocities. This is strong evidence for the existence of the upwelling of hot material caused by the subduction. These low-velocity anomalies are associated with volcanic activity, i.e., the Tengchong volcano, and is likely a result of the higher temperatures and/or partial melting associated with volcanism (Hearn and Ni, 1994). Low Pn velocity anomalies are also associated with the subduction in the Hindu Kush region as well. Here, the low velocity anomaly does not totally align with the volcanoes, but the distance between the volcanoes and the low velocity anomaly is not very large. The misalignment between the low velocity anomaly and the volcano distribution probably underscores the complexity of the crust at this region. Therefore, determining the detailed crustal structure from 3D tomography may help to illuminate the link between the volcanoes and the crustal velocity anomalies. It is widely accepted that the Indian Plate collided with the Asian Plate in the Tibetan Plateau, but the mechanism of subduction is still unclear. The cold lithosphere of the Indian Plate has a high Pn velocity, and this is confirmed in our inversion results. This high-velocity anomaly area roughly reaches the IYS. In the area north of the IYS suture, low Pn velocities were found. Zheng et al. (2007) proposed a model using teleseismic P-waves that the lithosphere of the Indian Plate subducted 200–300 km deep into the mantle. Our inversion results also support the theory that the lithosphere of the Indian Plate subducted into the mantle, causing the upwelling of hot material in the north of the IYS. In addition, the stable regions such as the Tarim and Sichuan basins have high Pn velocities, and the Pn velocity under the Songpan-Ganzi fold belt is significantly lower. The slow anomalies in the Yunnan-Myanmar region, the western part of the QTB and the Songpan-Ganzi fold belt, as well as the fast anomalies in the Tarim and Sichuan basins are consistent with previous studies (Liang et al., 2004; Pei et al., 2007). Our results also show that high Pn velocity anomalies in the Indian Plate are discontinuous at the collision region in the east-west direction, which suggests that the Indian Plate may subduct by different blocks. That is, the Indian plate probably does not subduct in one piece beneath Tibet, but rather in a piecewise manner. Liang et al. (2006) has also proposed that the Indian lithosphere advances northward in different pieces with different rates. As this discontinuous model may be affected by the uneven distribution of the ray paths or the trade-off between velocity and anisotropy, we believe that this conjecture demands more studies before confirmation.
We also obtained Pn velocities without the anisotropy effects for comparison (Fig. 5(b)). Both models share the following common features throughout most of the study area: high Pn velocities under the Indian Plate and in the Tarim basin, low Pn velocities under the Hindu Kush and in Myanmar and the adjacent region. We have also observed that the high Pn velocities in the Sichuan and Tarim basins are not as obvious as in the anisotropy model. Joint inversion with anisotropy helps to determine a more reliable velocity picture.
We present high-resolution Pn velocity and anisotropy models for the uppermost mantle beneath the Tibetan Plateau and the adjacent regions using large data sets and provide constraints on plate structure and the processes of continental deformation. The average Pn velocity under the study area is approximately 8.15 km/s, with maximum velocity perturbations of approximately 3–4%. We found high Pn velocities beneath the Indian Plate and in the Tarim and the Sichuan basins, low Pn velocities under Myanmar, its adjacent region and the Hindu Kush region, and especially low Pn velocities under the area north of the IYS. The cold lithosphere in the Indian Plate exhibits a high Pn velocity. The high Pn velocity anomalies of the Indian Plate are discontinuous at the collision region in the east-west direction, which may be related to the block subduction process of the Indian Plate, indicating that the Indian plate probably subducts in a piecewise manner. In the area north of the IYS, low Pn velocities are associated with the subduction of the Indian lithosphere. The regions that are stable and less affected by tectonic activities, such as the Tarim and Sichuan basins, have high Pn velocities, and the Pn velocity under the Songpan-Ganzi fold belt is significantly lower. At the plate collisions, the fast Pn anisotropy direction is parallel to the collision arc. The anisotropy at the plate boundary may be caused by shear strains along the boundary; the shear traction on the base of the lithosphere could orient the fast axis in olivine crystals parallel to the shear direction. The fast Pn anisotropy in the eastern Tibetan Plateau suggests that the preferred alignment of olivine crystals is parallel to the plate movement direction.
Our results agree well with previous models but provide a more detailed uppermost mantle structure in the study area. In the near future, we expect to further enhance the regional model by developing an Sn model to delineate structural details around the low velocity zones.
However, Pn and Sn models only provide information of the uppermost mantle and therefore offer limited information for crustal structures. Full 3D crustal P and S velocity models will definitely help to link surface geological features with tectonic processes at depth. With many more broadband seismic stations becoming available in Tibet and the adjacent regions, the recently-developed ambient noise tomography will help to provide more accurately-resolved crustal structures using short period surface waves as well as Moho-reflected body waves such as S m S (Yang et al., 2010; Zhan et al., 2010).
We would like to thank Thomas M. Hearn for providing the original tomographic idea and codes. We thank Dr. Pei Shunping for his valuable comments. We also appreciate the insightful suggestions by two reviewers. The data from the Chinese Earthquake Network catalog are downloaded from http://www.csndmc.ac.cn, and the ISC data from http://www.isc.ac.uk. This study is supported by the National Nature Science Foundation of China (Grant No. 41074031 and 40940021) and China Earthquake Program 200808078.
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