We have used high-resolution Mars Orbiter Laser Altimeter (MOLA) data to analyze the topography, morphology, stratigraphy, and geologic history of the Martian north circumpolar deposits. The present polar deposits are offset about toward 0øW from the rotational pole. An arc of irregular topography, concentric to Olympia Planitia and the cap, consists of polar material remnants, depressions which we interpret to be kettles, frost-covered and residual ice-filled craters, and frost patches. Olympia Planitia, originally thought to be a flat, sand-covered plain, is characterized by a convex-upward topography, contiguous with the polar cap. We interpret Olympia Planitia to represent a now dune-covered extension of the polar materials. Together, Olympia Planitia and the outlying deposits delineate a former extent of the polar cap. Topographic data have clarified relationships among the circumpolar deposits. Contributors to these deposits include local volcanics, fluvial and aqueous sediments (from outflow channels and a possible standing body of water), pyroclastic ash, sublimation lag from the Olympia Lobe, and eolian-reworked materials. Significant events in the history of the region include (1) formation of the northern lowlands; (2) emplacement of volcanic plains, fluvial and aqueous sedimentation, and subsequent desiccation, forming polygonal patterns which in part underlie the present polar layered deposits; (3) formation of the polar cap, composed primarily of layered deposits; (4) asymmetric retreat of the Olympia Lobe, resulting in sublimation lag deposits, polar remnants, and kettles; and (5) continued collection and reworking of sediments by eolian processes. The cause of the asymmetrical retreat of the Olympia Lobe is unknown. cinity of the base of the cap [Lucchitta et al., 1986]. While it has been postulated that the polar cap and its mapped patches of outlying residual ice remnants may be a major source for the north polar erg [Dial, 1984; Tanaka and Scott, 1987], the composition of the layered deposits within the polar cap and the thickness of the layers are not known to sufficient accuracy to substantiate this conclusion [Thomas et al., 1992]. Until the acquisition of high-resolution topographic data from the Mars Orbiter Laser Altimeter (MOLA)several factors concerning the mapped geologic units and complex geological processes have been difficult to constrain. These include the following: (1) the topography of the region as a whole and of the individual geologic units, (2) the stratigraphic relationpolar region [Dial, 1984; Tanaka and Scott, 1987; dager and ships of the geologic units and the source of the circumpolar Head, 1999]. The largest ergs on Mars reside within the cir-deposits, (3) the topographic nature of the outlying polar recumpolar deposits [Dial, 1984; Tanaka and Scott, 1987; sidual ice (or frost) remnants mapped by Dial [1984] and Greeley et al., 1992]. The main cap contains the largest known Tanaka and Scott [1987], and (4) the possibility that the cap reservoir of water on the planet ...