Relationship between the Tibetan Plateau–tropical Indian Ocean thermal contrast and the South Asian summer monsoon

doi:10.1007/s11707-020-0846-9

Front. Earth Sci.

2021, Vol. 15

Issue (1) : 151-166 https://doi.org/10.1007/s11707-020-0846-9

RESEARCH ARTICLE

Relationship between the Tibetan Plateau–tropical Indian Ocean thermal contrast and the South Asian summer monsoon

Xiaoqing LUO^1,², Jianjun XU^1,²(

), Yu ZHANG^1,², Kai LI³

¹. South China Sea Institute of Marine Meteorology, Guangdong Ocean University, Zhanjiang 524088, China
². College of Ocean and Meteorology, Guangdong Ocean University, Zhanjiang 524088, China
³. Maritime College, Guangdong Ocean University, Zhanjiang 524088, China

Download: PDF(4820 KB) HTML
Export: BibTeX | EndNote | Reference Manager | ProCite | RefWorks

Abstract

The impact of land–sea thermal contrast on the South Asian summer monsoon (SASM) was investigated by calculating the atmospheric heat sources (AHS) and baroclinic component with ERA5 data for the period 1979–2019. Using diagnostic and statistical methods, it was found that the thermal contrast between the Tibetan Plateau (TP) and the tropical Indian Ocean (TIO) affects the South Asian monsoon circulation through the meridional temperature gradient in the upper troposphere. The seasonal changes of the AHS of the TP and TIO are reversed. In summer, the TP is the strongest at the same latitude whereas the TIO is the weakest, and the thermal contrast is the most obvious. The heat sources of the TP and TIO are located on the north and south side of the strong baroclinic area of the SASM region, respectively, and both of which are dominated by deep convective heating in the upper troposphere. The TP–TIO regional meridional thermal contrast index (QI) based on the AHS, and the SASM index (MI) based on baroclinicity were found to be strongly positively correlated. In years of abnormally high QI, the thermal contrast between the TP and TIO is strong in summer, which warms the upper troposphere over Eurasia and cools it over the TIO. The stronger temperature gradient enhances the baroclinicity in the troposphere, which results in a strengthening of the low-level westerly airflow and the upper-level easterly airflow. The anomalous winds strengthen the South Asian high (SAH), with the warmer center in the upper troposphere, and the enhanced Walker circulation over the equatorial Indian Ocean. Finally, the anomalous circulation leads to much more precipitation over the SASM region. The influence of abnormally low QI is almost the opposite.

Keywords Tibetan Plateau tropical Indian Ocean atmosphere heat sources South Asian summer monsoon atmosphere baroclinic component

Corresponding Author(s): Jianjun XU

Online First Date: 19 March 2021 Issue Date: 19 April 2021

Cite this article:

Xiaoqing LUO,Jianjun XU,Yu ZHANG, et al. Relationship between the Tibetan Plateau–tropical Indian Ocean thermal contrast and the South Asian summer monsoon[J]. Front. Earth Sci., 2021, 15(1): 151-166.

URL:

https://academic.hep.com.cn/fesci/EN/10.1007/s11707-020-0846-9
https://academic.hep.com.cn/fesci/EN/Y2021/V15/I1/151

Fig.1 Study area, showing the topography (shaded; unit: m) of the Tibetan Plateau (TP; 75°E–103°E, 28°N–38°N; altitude≥3000 m; bordered in red), the tropical Indian Ocean (TIO; 60°E–100°E, 15°S–5°N; red box) and the South Asian monsoon region (SAM, 40°E–100°E, 0°–20°N; black box).

Fig.2 Seasonal variations of the zonal anomaly of Q1 (shaded; units: W/m²) and K_s≥60 m/s (black curve). MAM (March–April–May), JJA (June–July–August), SON (September–October–November) and DJF (December–January–February) represent spring, summer, autumn and winter, respectively. The Tibetan Plateau (≥3000 m) is outlined in green; the tropical Indian Ocean is indicated by the green box.

Fig.3 Zonal mean of (a) Q1 and (b) Q2 (units: W/m²). The Tibetan Plateau (TP≥3000 m) is located at 28°N–38°N; the tropical Indian Ocean (TIO) is located at 15S°–5°N; MAM (March–April–May), JJA (June–July–August), SON September–October–November) and DJF (December–January–February) represent spring, summer, autumn and winter, respectively; and altitude is shaded black (unit: km).

Fig.4 Vertical profiles of summer Q₁ and Q₂ at 90°E. The Tibetan Plateau is represented by the dotted curve at 28°N–38°N, and the TIO by the solid curve at 15°S–5°N;

Q 1 t

Q 1 v

and

Q 1 w

represent the time tendency, horizontal advection and vertical advection, respectively, and likewise for Q₂.

Fig.5 The 400–200-hPa time–meridional variations of (a) Q₂, (b) Q_2t, (c) Q_2w and (d) temperature at 70°E–100°E(Q_2t, and Q_2w represent the time tendency and vertical advection, respectively).

Fig.6 Zonal temperature anomaly at 400–200 hPa (red curve, unit: K), 200-hPa geopotential≥12500 gpm (black curve), and outgoing longwave radiation (shaded; units: W/m²) in summer. The Tibetan Plateau (≥3000 m) is outlined in green; the tropical Indian Ocean is indicated by the green box.

Fig.7 Seasonal variations of QI(solid black line), QI_up (black dotted line), TI_up (purple line) and MI (red line) (see subsection 2.2(2) in the main text for definitions of these indexes). The Q₁ in the TP and TIO is denoted in orange and blue, respectively, and all data have been detrended and standardized.

Fig.8 Evaluation of the SASM, in which (a–f) represent May–October, respectively, with precipitation shaded (units: mm/day). The wind vectors are at 850 hPa (units: m/s); the K_s≥60 m/s is outlined in red; the Tibetan Plateau is outlined in blue (altitude≥3000 m); and the tropical Indian Ocean is denoted by the blue box.

Fig.9 Seasonal–zonal profiles at 15°N of (a) zonal wind at 850 hPa, (b) meridional wind at 200 hPa, (c) Q₁, and (d) precipitation. Shading in (a, c) represents values≥0; in (b) it represents v≤0; and in (d) Pre≥0.

Fig.10 Temporal variations of the summer QI, TI_up, QI_up and MI (see section 2.2. (2) for definitions of these indexes; all data have been detrended and standardized).

Fig.11 Anomalous temperature at 400–200 hPa (shaded; unit: K; dotted areas pass the 90% significance test) and K_s (≥60 m/s). Pos represents QI≥1; Neg represents QI<1. The Tibetan Plateau (≥3000 m) is outlined in green; the tropical Indian Ocean is denoted by the green box.

Fig.12 Seasonal profiles of the difference in anomalous temperature at 400–200 hPa between 30°N and 5°N. Pos represents QI≥1; Neg represents QI<1; shaded area represents temperature≥6 K.

Fig.13 Vertical–meridional profiles of the anomalous Q₁ (shaded) and K_s (curve) in summer. The mean is at 80°E–96°E; Pos represents QI≥1; Neg represents QI<1; and black shading and blue dotted line represent the topography and TP respectively).

	$K s u$			$K s v$
	Nor	Pos	Neg	Nor	Pos	Neg
Jun	66.40	70.53	66.40	19.98	21.23	19.15
Jul	80.10	80.84	80.10	22.19	22.37	21.17
Aug	74.74	78.00	74.74	19.98	21.11	19.44
mean	73.75	76.45	73.75	20.71	21.57	19.92

Tab.1 The anomalies of K_su and K_sv in summer. Pos represents QI≥1; Neg represents QI<1; Nor represents the normal

Tab.2 Correlation coefficients between the thermal contrast index and MI.

Fig.14 Regression of TI_up, K_s and T_2m on QI in summer. Shaded areas pass the 95% significance test; the Tibetan Plateau (≥3000 m) is outlined in green; and the tropical Indian Ocean is denoted by the green box.

Fig.15 The 850-hPa u-component (a) and 200-hPa v-component in summer at 15°N (b). Pos represents QI≥1; Neg represents QI<1; Nor represents the norm; and shading indicates v≤0.

Fig.16 Abnormal winds at 850 hPa (a1, b1), 200 hPa in summer (a2, b2) and the K_s (red curve). Pos represents QI≥1; Neg represents QI<1; wind vectors pass the 95% significance test; the Tibetan Plateau (≥3000 m) is outlined in green; the tropical Indian Ocean is denoted by the green box; and blue box represent 90°E–110°E, 23°N–38°N.

Fig.17 Vertical–zonal profiles of anomalous u–w winds (vectors) and the Q₁ (shaded) in summer at 0°–20°N. Pos represents QI≥1; Neg represents QI<1; and black shading denotes the topography.

Fig.18 Difference in summer precipitation in the Asian monsoon region between positive and negative QI (units: mm/day; plus signs indicate areas passing the 95% significance test; and black line and red line (geopotential≥12500 gpm) represents the SAH area of QI≥1 and QI<1 respectively; and black line and red line (geopotential≥12553 gpm) represents the SAH center of QI≥1 and QI<1 respectively).

1	C Chou (2003). Land-sea heating contrast in an idealized Asian summer monsoon. Clim Dyn, 21(1): 11–25 https://doi.org/10.1007/s00382-003-0315-7
2	A G Dai, H M Li, Y Sun, L C Hong, L Ho, C Chou, T J Zhou (2013). The relative roles of upper and lower tropospheric thermal contrasts and tropical influences in driving Asian summer monsoons. J Geophys Res, 118(13): 7024–7045 https://doi.org/10.1002/jgrd.50565
3	A M Duan, G X Wu (2005). Role of the Tibetan Plateau thermal forcing in the summer climate patterns over subtropical Asia. Clim Dyn, 24(7–8): 793–807 https://doi.org/10.1007/s00382-004-0488-8
4	C Fu, J O Fletcher (1985). The relationship between Tibet-tropical ocean thermal contrast and interannual variability of Indian monsoon rainfall. J Appl Meteorol, 24(8): 841–847 https://doi.org/10.1175/1520-0450(1985)024<0841:TRBTTO>2.0.CO;2
5	B N Goswami, V Krishnamurthy, H Annmalai (1999). A broad-scale circulation index for the interannual variability of the Indian summer monsoon. Q J R Meteorol Soc, 125(554): 611–633 https://doi.org/10.1002/qj.49712555412
6	Z Y Guan, J J Xu, P W Guo, C Wang (1997). The structure and variations of Asian summer monsoon reveled by barotropic and baroclinic modes the baroclinic mode analysis. Acta Meteorol Sin, 55(02): 19–26 (in Chinese)
7	Z Guan (2000). The variations of Asian monsoon as revealed by the variations of kinetic energy of barotropic/baroclinic modes of the wind field. Transactions of Atmospheric Sciences, 23(03): 313–322 (in Chinese)
8	J Hansen, R Ruedy, M Sato, K Lo (2010). Global surface temperature change. Rev Geophys, 48(4): RG4004 https://doi.org/10.1029/2010RG000345
9	H Y He, C H Sui, M Q Jian, Z P Wen, G Lan (2003). The evolution of tropospheric temperature field and its relationship with the onset of Asian summer monsoon. J Meteorol Soc Jpn, 81(5): 1201–1223 https://doi.org/10.2151/jmsj.81.1201
10	Y L He, J P Huang, M J Ji (2014). Impact of land–sea thermal contrast on interdecadal variation in circulation and blocking. Clim Dyn, 43(12): 3267–3279 https://doi.org/10.1007/s00382-014-2103-y
11	H Hersbach, B Bell, P Berrisford, S Hirahara, A Horányi, J Muñoz-Sabater, J Nicolas, C Peubey, R Radu, D Schepers, A Simmons, C Soci, S Abdalla, X Abellan, G Balsamo, P Bechtold, G Biavati, J Bidlot, M Bonavita, G De Chiara , P Dahlgren, D Dee, M Diamantakis, R Dragani, J Flemming, R Forbes, M Fuentes, A Geer, L Haimberger, S Healy, R J Hogan, E Hólm, M Janisková , S Keeley, P Laloyaux, P Lopez, C Lupu, G Radnoti, P de Rosnay, I Rozum, F Vamborg, S Villaume, J Thépaut (2020). The ERA5 global reanalysis. Q J R Meteorol Soc, 146(730): 1999–2049.
12	J Y Huang, Q X Li (2015). Methods for Statistical Analysis of Meteorological Data. Beijing: Meteorology Press (in Chinese)
13	J R, Holton G J Hakim (2004). An Introduction to Dynamic Meteorology. Burlington: Elsevier Acad
14	R H Kripalani, A Kulkarni, S S Sabade, M L Khandekar (2003). Indian Monsoon variability in a global warming scenario. Nat Hazards, 29(2): 189–206 https://doi.org/10.1023/A:1023695326825
15	C F Li, M Yanai (1996). The onset and interannual variability of the Asian summer monsoon in relation to land-sea thermal contrast. J Clim, 9(2): 358–375 https://doi.org/10.1175/1520-0442(1996)009<0358:TOAIVO>2.0.CO;2
16	J P Li, Q C Zeng (2002). A unified monsoon index. Geophys Res Lett, 29(8): 115–1–115–4.
17	B, Liebmann C A Smith (1996). Description of a complete (interpolated)— outgoing longwave radiation dataset. Bull Amer Meteor Soc, 77(6): 1275–1277
18	X Liu, G X Wu, Y M Liu, P Liu (2002). Diabatic heating over the Tibetan Plateau and seasonal variastions of the Asian Circulation and summer monsoon. Chin J Atmos Sci, 6: 781–793 (in Chinese)
19	X Liu, M Yanai (2001). Relationship between the Indian monsoon rainfall and the tropospheric temperature over the Eurasia Continent. Q J R Meteorol Soc, 127(573): 909–937 https://doi.org/10.1002/qj.49712757311
20	Y M Liu, G X Wu, J L Hong, B W Dong, A M Duan, Q Bao, T J Zhou (2012). Revisiting Asian monsoon formation and change associated with Tibetan Plateau forcing: I. Formation. Clim Dyn, 39(5): 1169–1181 https://doi.org/10.1007/s00382-012-1335-y
21	Y M Liu, G X Wu, H Liu, P Liu (1999). The effect of spatially nonuniform heating on the formation and variation of subtropical high part III: condensation heating and south Asia high and western Pacific. Acta Meteorol Sin, 57(5): 525–538 (in Chinese)
22	X Q Luo, J J Xu (2019). Estimate of atmospheric heat source over Tibetan Plateau and its uncertainties. Climate Change Research, 15(1): 33–40 (in Chinese)
23	X Q Luo, J J Xu, K Li (2019). A review of atmospheric heat sources over the Tibetan Plateau. J Guangdong Ocean Univ, 39(06): 130–136 (in Chinese)
24	G Naveendrakumar, M Vithanage, H H Kwon, S S K Chandrasekara, M C Iqbal, S Pathmarajah, W C D K Fernando, J Obeysekera (2019). South Asian perspective on temperature and rainfall extremes: a review. Atmos Res, 225: 110–120 https://doi.org/10.1016/j.atmosres.2019.03.021
25	B Parthasarathy, K R Kumar, D R Kothawale (1992). Indian summer monsoon rainfall indices: 1871–1990. Meteorological Magazine, 121(1441): 174–186
26	M K Roxy, K Ritika, P Terray, R Murtugudde, K Ashok, B N Goswami (2015). Drying of Indian subcontinent by rapid Indian Ocean warming and a weakening land-sea thermal gradient. Nat Commun, 6(1): 7423 https://doi.org/10.1038/ncomms8423 pmid: 26077934
27	N A Sontakke, G B Pant, N Singh (1993). Construction of all-India summer monsoon rainfall series for the period 1844–1991. J Clim, 6(9): 1807–1811 https://doi.org/10.1175/1520-0442(1993)006<1807:COAISM>2.0.CO;2
28	X R Sun, L X Chen, J H He (2002). Index of the sea thermal difference and its relation to interannual variation of summer circulation and rainfall over East Asian. Acta Meteorol Sin, 60(02): 164–172 (in Chinese)
29	Y Sun, Y H Ding, A G Dai (2010). Changing links between South Asian summer monsoon circulation and tropospheric land-sea thermal contrasts under a warming scenario, Geophys Res Lett, 37(2):195–205
30	A G Turner, H Annamalai (2012). Climate change and the South Asian summer monsoon. Nat Clim Chang, 2(8): 587–595 https://doi.org/10.1038/nclimate1495
31	H W Tu, H Y Tian, X Xu, R Zhang (2020). Influence of the south-north displacement of South Asia High on the distribution of atmospheric composition in the upper troposphere-lower stratosphere over the Asian Monsoon Region. Plateau Meteorol, 39(2): 333–346
32	B Wang, Z Fan (1999). Choice of South Asian summer monsoon indices. Bull Am Meteorol Soc, 80(4): 629–638 https://doi.org/10.1175/1520-0477(1999)080<0629:COSASM>2.0.CO;2
33	B Wang, J Liu, H J Kim, P J Webster, S Y Yim, B Xiang (2013). Northern Hemisphere summer monsoon intensified by mega-El Nino/southern oscillation and Atlantic multidecadal oscillation. Proc Natl Acad Sci USA, 110(14): 5347–5352 https://doi.org/10.1073/pnas.1219405110 pmid: 23509281
34	P X Wang, B Wang, H Cheng, J Fasullo, Z T Guo, T Kiefer, Z Y Liu (2017). The global monsoon across time scales: mechanisms and outstanding issues. Earth Sci Rev, 174: 84–121 https://doi.org/10.1016/j.earscirev.2017.07.006
35	Y N Wang, B Zhang, L X Chen, J H He, W Li, H Chen (2008). Relationship between the atmospheric heat source over Tibetan Plateau and the heat source and general circulation over East Asia. Sci Bull (Beijing), 53(21): 3387–3394 https://doi.org/10.1007/s11434-008-0327-0
36	P J Webster, V O Magaña, T N Palmer, J Shukla, R A Tomas, M Yanai, T Yasunari (1998). Monsoons: processes, predictability, and the prospects for prediction. J Geophys Res D Atmospheres, 103(C7): 14451–14510 https://doi.org/10.1029/97JC02719
37	P J Webster, S Yang (1992). Monsoon and Enso: selectively interactive systems. Q J R Meteorol Soc, 118(507): 877–926 https://doi.org/10.1002/qj.49711850705
38	W Wei (2015). The interannual shift of the South Asia High and its relation with the Asian summer monsoon. Dissertation for the Doctoral Degree. Beijing: Chinese Academy of Meteorological Sciences (in Chinese)
39	G X Wu, A M Duan, Y M Liu, J H Yang, B Q Liu, S L Ren, Y N Zhang, T M Wang, X Y Liang, Y Guan(2013). Recent advances in the study on the dynamics of the Asian summer monsoon onset. Chin J Atmos Sci, 37(2): 211–228 (in Chinese)
40	G X Wu, H Bian, Y M Liu, Q Bao, R C Ren, B Q Liu (2016). Recent progresses on dynamics of the Tibetan Plateau and Asian summer monsoon. Chin J Atmos Sci, 40(1): 22–32 (in Chinese)
41	G Wu, Y Liu (2003). Summertime quadruplet heating pattern in the subtropics and the associated atmospheric circulation. Geophys Res Lett, 30(5): 5–1 https://doi.org/10.1029/2002GL016209
42	G Wu, Y Liu, B He, Q Bao, A Duan, F F Jin (2012). Thermal controls on the Asian summer monsoon. Sci Rep, 2(1): 404 https://doi.org/10.1038/srep00404 pmid: 22582141
43	G X Wu, Y M Liu, X Liu, A M Duan, X Y Liang(2005). How the heating over the Tibetan Plateau affects the Asian climate in summer. Chinese Journal of Atmospheric Sciences, 29(1):47–56+167–168 (in Chinese)
44	J J Xu, J C L Chan (2002). Relationship between the planetary—scale circulation over East Asia and the intensity of the South Asian Summer Monsoon. Geophys Res Lett, 29(18): 1866 https://doi.org/10.1029/2002GL014918
45	M Yanai, C F Li Z S , Song (1992). Seasonal heating of the Tibetan Plateau and its effects on the evolution of the Asian summer monsoon. J Meteorol Soc Jpn, 70(1B): 319–351 https://doi.org/10.2151/jmsj1965.70.1B_319
46	M Yanai, T Tomita (1998). Seasonal and interannual variability of atmospheric heat sources and moisture sinks as determined from NCEP–NCAR reanalysis. J Clim, 11(3): 463–482 https://doi.org/10.1175/1520-0442(1998)011<0463:SAIVOA>2.0.CO;2
47	M Yanai, G X Wu (2006). Effects of the Tibetan plateau. In: The Asian Monsoon. Heidelberg: Springer, 513–549
48	Q You, J Min, W Zhang, N Pepin, S Kang (2015). Comparison of multiple datasets with gridded precipitation observations over the Tibetan Plateau. Clim Dyn, 45(3–4): 791–806 https://doi.org/10.1007/s00382-014-2310-6
49	Y Zhang, G Fan, W Hua, Y Zhang, B Wang, X Lai (2017). Differences in atmospheric heat source between the Tibetan Plateau–South Asia region and the southern Indian Ocean and their impacts on the Indian summer monsoon outbreak. J Meteorol Res, 31(3): 540–554 https://doi.org/10.1007/s13351-017-6042-5
50	R F Zhan, J P Li (2008). The effect of atmospheric heat source in the Tibetan Plateau and the tropical Northwest Pacific Ocean on the interdecadal variation of summer stratospheric-tropospheric water vapor exchange in Asia. Sci China Ser D Earth Sci, 38(8): 1028–1040(in Chinese)
51	Y Zhao, A M Duan, G X Wu, R Z Sun (2019). Response of the Indian ocean to the Tibetan Plateau thermal forcing in late spring. J Clim, 32(20): 6917–6938 https://doi.org/10.1175/JCLI-D-18-0880.1

[1]	Zhengjia LIU,Mei HUANG. *Assessing spatio-temporal variations of precipitation-use efficiency over Tibetan grasslands using MODIS and in-situ* observations**[J]. Front. Earth Sci., 2016, 10(4): 784-793.
[2]	Tongtiegang ZHAO,Jianshi ZHAO,Hongchang Hll,Guangheng NI. Source of atmospheric moisture and precipitation over China’s major river basins[J]. Front. Earth Sci., 2016, 10(1): 159-170.
[3]	Hongxia LIU,Ying HU,Shihua QI,Xinli XING,Yuan ZHANG,Dan YANG,Chengkai QU. Organochlorine pesticide residues in surface water from Sichuan Basin to Aba Prefecture profile, east of the Tibetan Plateau[J]. Front. Earth Sci., 2015, 9(2): 248-258.
[4]	Hongxia LIU, Shihua QI, Dan YANG, Ying HU, Feng LI, Jia LIU, Xinli XING. Soil concentrations and soil-air exchange of organochlorine pesticides along the Aba profile, east of the Tibetan Plateau, western China[J]. Front Earth Sci, 2013, 7(4): 395-405.
[5]	Jian YANG, Hongchen JIANG, Geng WU, Weiguo HOU, Yongjuan SUN, Zhongping LAI, Hailiang DONG. Co-occurrence of nitrite-dependent anaerobic methane oxidizing and anaerobic ammonia oxidizing bacteria in two Qinghai-Tibetan saline lakes[J]. Front Earth Sci, 2012, 6(4): 383-391.
[6]	Fang HAN, Kexin ZHANG, Junliang JI, Yadong XU, Fenning CHEN, Xiaohu KOU. Late Pleistocene sedimentary sequences and paleoclimate changes in Xunhua basin in the upper reach of Yellow River in China[J]. Front Earth Sci, 2012, 6(3): 297-305.
[7]	Furong LI, Yan ZHAO, Jinghui SUN, Wenwei ZHAO, Xiaoli GUO, Ke ZHANG. Surface pollen and its relationship to vegetation in the Zoige Basin, eastern Tibetan Plateau[J]. Front Earth Sci, 2011, 5(3): 252-261.
[8]	Rongke XU, Xiongfei CAI, Yulian ZHANG, Liang SHAN, Yaoyu CHEN, Jianhong QI, Gang WANG, . Impact of phased uplift of Tibetan Plateau on environmental changes since late Middle Pleistocene: Palynological records in the three terraces of Middle Shiquan River[J]. Front. Earth Sci., 2009, 3(4): 402-410.
[9]	GUO Zhengfu, CHEN Xiaoyu, LIU Jiaqi. Effect of volatiles erupted from Mesozoic and Cenozoic volcanic activities on paleo-environmental changes in China[J]. Front. Earth Sci., 2008, 2(4): 393-396.
[10]	FAN Daidu, LI Congxian. Timing of the Yangtze initiation draining the Tibetan Plateau throughout to the East China Sea: a review[J]. Front. Earth Sci., 2008, 2(3): 302-313.
[11]	ZHAO Zhizhong, QIAO Yansong, WANG Shubing, YAO Haitao, WANG Yan, FU Jianli, LI Chaozhu, LIU Zongxiu, JIANG Fuchu. Geological characteristics and evolution of the eastern Qinghai-Tibetan plateau since the late Cenozoic[J]. Front. Earth Sci., 2008, 2(2): 209-216.
[12]	WEI Hualing, FANG Nianqiao, DING Xuan, LIU Xiuming, NIE Lanshi. Pelagic records from the Equatorial Ninetyeast Ridge and significant environmental events during the past 3.5 Ma[J]. Front. Earth Sci., 2008, 2(2): 162-169.

Viewed

Full text

Abstract

Cited

Shared

Discussed