Acceso abierto

Electron Spin Resonance (ESR) Signal Intensity of Quartz E1′ Centre and Its Potential Use in Fluvial Sediments Provenance Tracing

Chuan-Yi Wei

Chuan-Yi Wei

  • State Key Laboratory of Earthquake Dynamics, Institute of Geology, China Earthquake AdministrationBeijing, China
  • School of Earth Sciences, China University of GeosciencesWuhan, China
Buscar este autor en
Sciendo|Google Scholar
Wei, Chuan-Yi
, 
Chun-Ru Liu

Chun-Ru Liu

State Key Laboratory of Earthquake Dynamics, Institute of Geology, China Earthquake AdministrationBeijing, China
Buscar este autor en
Sciendo|Google Scholar
Liu, Chun-Ru
, 
Gong-Ming Yin

Gong-Ming Yin

State Key Laboratory of Earthquake Dynamics, Institute of Geology, China Earthquake AdministrationBeijing, China
Buscar este autor en
Sciendo|Google Scholar
Yin, Gong-Ming
 y 
Wen-Peng Li

Wen-Peng Li

  • State Key Laboratory of Earthquake Dynamics, Institute of Geology, China Earthquake AdministrationBeijing, China
  • Department of Ocean Science and Engineering, Southern University of Science and TechnologyShenzhen, China
Buscar este autor en
Sciendo|Google Scholar
Li, Wen-Peng
  
31 dic 2021
Electron Spin Resonance (ESR) Signal Intensity of Quartz E1′ Centre and Its Potential Use in Fluvial Sediments Provenance Tracing's Cover Image
Acerca de este artículo
Artículo anterior
Artículo siguiente
Cite
Descargar portada
Categoría del artículo: Conference Proceedings of the 5Asia Pacific Luminescence and Electron Spin Resonance Dating Conference October 15–17, 2018, Beijing, China. Guest Editor: Liping Zhou
Publicado en línea: 31 dic 2021
Páginas: 197 - 204
Recibido: 08 ene 2019
Aceptado: 02 abr 2020
DOI: https://doi.org/10.2478/geochr-2020-0040
Palabras clave
© 2019 Chuan-Yi Wei et al., published by Sciendo
This work is licensed under the Creative Commons Attribution-NonCommercial-NoDerivatives 3.0 License.

Fig. 1

Map showing study area and geological setting of sampling sites. (a) and (b) show study area located in the eastern Tibetan Plateau. (c) show geological setting and sampling site of Kang’ding River and Diao’tengzi River. The Pan’zhihua River and the Mian’ning River are marked as two black circles on 1–(b). The source rock age data are from China Intrusive Rock Isotope Age Atlas by K-Ar dating method.
Map showing study area and geological setting of sampling sites. (a) and (b) show study area located in the eastern Tibetan Plateau. (c) show geological setting and sampling site of Kang’ding River and Diao’tengzi River. The Pan’zhihua River and the Mian’ning River are marked as two black circles on 1–(b). The source rock age data are from China Intrusive Rock Isotope Age Atlas by K-Ar dating method.

Fig. 2

Typical E1’ centre ESR spectrum of quartz in this study.
Typical E1’ centre ESR spectrum of quartz in this study.

Fig. 3

The heat-treated E1’ signal intensity response to heating temperatures. The similar changes upon heating indicate that the heat-treated E1’ signal intensity of quartz extracted from fluvial sediment can reach the maximum value at about 300°C for 15 min. However, the maximum heat-treated E1’ signal intensity varies in quartz with different formation ages. For example, PZH03 reaches the maximum value at 300°C while DTZG03 at 330°C. Above about 400°C, the E1’ signal intensity of PZH03 and DTZG03 are zero.
The heat-treated E1’ signal intensity response to heating temperatures. The similar changes upon heating indicate that the heat-treated E1’ signal intensity of quartz extracted from fluvial sediment can reach the maximum value at about 300°C for 15 min. However, the maximum heat-treated E1’ signal intensity varies in quartz with different formation ages. For example, PZH03 reaches the maximum value at 300°C while DTZG03 at 330°C. Above about 400°C, the E1’ signal intensity of PZH03 and DTZG03 are zero.

Fig. 4

Correlation between heat-treated E1’ signal intensity of quartz in source rock and its fluvial sediments heated at 300°C (a) and 330°C (b).
Correlation between heat-treated E1’ signal intensity of quartz in source rock and its fluvial sediments heated at 300°C (a) and 330°C (b).

Fig. 5

Correlation between rock age and its heat-treated E1’ signal intensity. (a) heating temperature is 300°C; (b) heating temperature is 330°C.
Correlation between rock age and its heat-treated E1’ signal intensity. (a) heating temperature is 300°C; (b) heating temperature is 330°C.

Sample information used in this study_

No. Drainage Sample name Sample type Latitude (°N) Longitude (°E) Rock age and dating method used
1 Mian’ning River MN05 modern river sediments 28°31′30″ 102°03′42″ 134 Ma (kb)
2 MN06 bedrocks 28°31′30″ 102°03′42″ 134 Ma (kb)
3 Kang’ding River KD05 bedrocks 29°54′34″ 101°57′24″ 227 Ma (kb)
4 KD06 modern river sediments 29°59′42″ 101°56′50″ 227 Ma (kb)
5 Pan’zhihua River PZH01 bedrocks 26°25′21″ 101°44′00″ 783 Ma (uz)
6 PZH03 modern river sediments 26°25′28″ 101°44′48″ 783 Ma (uz)
7 Diao’tengzi River DTZG03 historical sediments 29°16′01″ 102°18′26″ 821 Ma (kw)
8 DTZG04 modern river sediments 29°16′01″ 102°18′26″ 821 Ma (kw)

Difference of quartz heat-treated E1’ signal intensity between sediment and its source rock_

drainage heating temperature (°C) heat-treated E1′ signal intensity |(A-B)| (A+B)/2 difference value (%)
sediment source rock
Mian’ning River 300 1.06 1.22 0.16 1.14 14
330 1.06 1.21 0.15 1.135 13
Kang’ding River 300 2.60 2.36 0.24 2.48 10
330 2.61 2.36 0.25 2.49 10
Pan’zhi’hua River 300 6.75 6.31 0.44 6.53 7
330 6.74 6.30 0.44 6.52 7
Diao’teng’zi River 300 8.82 9.64 0.82 9.23 9
330 11.92 10.58 1.34 11.25 12
Idioma:
Inglés
Calendario de la edición:
1 veces al año
Temas de la revista:
Geociencias, Geociencias, otros
RSS Feed de revista