The small components of the Earth daytime mesosphere and lower thermosphere (MLT) O(3P), O3 and CO2 are responsible for the thermal regime of the MLT region. Based on YM2011 model of kinetics of excited products of O3 and O2 photolysis in the MLT of the Earth we proposed and justified the methods of retrieving the atomic oxygen and ozone vertical distributions from the observation of emissions of the excited oxygen molecules and O(1D) atom. In the YM2011 model the processes of energy transfer among electronically-vibrationally excited singlet levels О2(b1Σ, v=0–2), O2(a1Δ, v=0–5), vibrationally excited levels O2(X3Σ, v=1–35) of the O2 molecules in the ground electronic state, and also excited atomic oxygen O(1D) were considered. For these excited levels the corresponding system of 45 kinetic balance equations was solved. Besides the O3 photolysis in Hartley spectral band, we also considered the photolysis in the Chappuis, Huggins, and Wulf spectral bands in the interval of 200−900 nm and the photolysis of O2 in Schumann–Runge continuum and Lyman-alpha line H atom, as well as resonant absorption of solar radiation in 629, 688 and 762 nm bands by O2. Using a sensitivity study and uncertainty analysis of the contemporary model of O3 and O2 photolysis in the MLT, YM2011, we determined that populations of four excited electronic-vibrational levels О2(b1Σ, v = 0 - 2), O2(a1Δ, v=0) and of metastable O(1D) atom depend on [O(3P)] and [O3] concentrations. We have tested all five excited components as the proxies of [O3] and [O(3P)] in the MLT region. For [O(3P)] altitude profile retrieval any from these 5 proxies can be used for different altitude range. Four proxies - О2(b1Σ, v = 0, 1), O2(a1Δ, v=0) and O(1D) are suitable for retrieving the altitude [O3] profile in the range of 50-100 km. In the interval 85 – 100 km the problem of independent and simultaneous retrieval of [O3] and [O(3P)] can be solved by using individual proxy for each of the target component. Commonly used [O3] retrieval proxy O2(a1Δ, v=0), transition from which forms the 1.27 μm O2 IR Atmospheric band, has more than one hour photochemical lifetime in the MLT region. On the other hand, the O(1D) and О2(b1Σ, v = 0 - 2) lifetime in the altitude region of 50−140 km is less than 14 sec. So, the proposed О2(b1Σ, v = 0 - 2) and O(1D) proxies can be used for tracking fast variations of the O3 and O(3P) atmospheric concentrations generated by wave processes and electron precipitations, and so on, when the O2(a1Δ, v=0) proxy becomes useless.