Paleointensity determination of Late Cretaceous basalts in northwest South Korea: implications for low and stable paleofield strength in the Late Cretaceous

Earth, Planets and Space

Table 3. Mean virtual (axial) dipole moment during the Late Cretaceous for each rock type.

Age interval (Ma)	N	VDMorVADM (× 10²² Am²)	References
Crystalline volcanic rock ^a
100–83	17 (13)	4.0±;2.1 (4.3±;2.3)	[1]–[5]
83–65	13 (5)	4.0±;1.6 (4.2±;0.9)	[5], [16], [17], this study
Submarine basaltic glass
100–83	47 (31)	7.2±;4.3 (7.3±;4.0)	[6]–[9]
83–65	19 (3)	7.1±;4.0(6.5±;2.2)	[6], [7]
Plutonic rocks (gabbro and dolerite)
100–83	22 (20)	6.2±;2.4 (6.4±;2.3)	[10]–[12]
83–65	1 (—)	4.0 (—)	[16]
Single plagioclase crystal
100–83	8 (8)	12.7±;0.7 (12.7±;0.7)	[13]
83–65	— (—)	— (—)	—
Sedimentary rocks of baked contact
100–83	5 (4)	4.5±;1.1 (4.9±;0.7)	[14], [15]
83–65	— (—)	— (—)	—
All rock types
100–83	99 (76)	6.7±;3.9 (7.0±;3.7)	[1]–[15]
83–65	33 (8)	5.8±;3.5 (5.1±;1.8) [5]–[7], [16], [17], this study	[5]–[7], [16], [17], this study

N: the number of cooling units used in calculating mean virtual (axial) dipole moment. The values in parentheses are calculated from a more rigorously selected paleointensity data set (see text for details). [1] Sherwood et al. (1993), [2] Tanaka and Kono (2002), [3] Zhao et al. (2004), [4] Riisager et al. (2001), [5] Shcherbakova et al. (2007), [6] Tauxe (2006), [7] Juárez et al. (1998), [8] Tauxe and Staudigel (2004), [9] Pick and Tauxe (1993), [10] Shcherbakova et al. (2012), [11] Granot et al. (2007), [12] Thomas et al. (2000), [13] Tarduno et al. (2002), [14] Shcherbakova et al. (2008), [15] Shcherbakova et al. (2009), [16] Perrin et al. (1999), [17] Goguitchaichvili et al. (2004).
^aCrystalline volcanic rock excludes submarine basaltic glass, even though basaltic glass occasionally includes crystalline particles (e.g., SD magnetite).